Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98

By GREGORY O. MENDEZ, WESLEY R. DANSKIN, and CARMEN A. BURTON

U.S. GEOLOGICAL SURVEY

Water-Resources Investigations Report 00-4269

Prepared in cooperation with the

SAN BERNARDINO VALLEY MUNICIPAL WATER DISTRICT 5020-74

Sacramento, California 2001 U.S. DEPARTMENT OF THE INTERIOR GALE A. NORTON, Secretary

U.S. GEOLOGICAL SURVEY Charles G. Groat, Director

The use of firm, trade, and brand names in this report is for identification purposes only and does not constitute endorsement by the U.S. Geological Survey.

For additional information write to: Copies of this report can be purchased from:

District Chief U.S. Geological Survey U.S. Geological Survey Information Services Placer Hall, Suite 2012 Box 25286 6000 J Street Federal Center Sacramento, CA 95819-6129 Denver, CO 80225 CONTENTS

Abstract...... 1 Introduction ...... 1 Purpose and Scope...... 2 Methods of Investigation ...... 3 Previous Investigations ...... 7 Acknowledgments ...... 8 Description of Study Area ...... 8 Physiography ...... 8 Population and Climate ...... 8 Geology ...... 9 Hydrology...... 9 Land Use...... 11 Water Use...... 16 Water Quality...... 16 Surface Water...... 16 Ground Water...... 22 Flowmeter Data ...... 26 Depth-Dependent Samples ...... 28 Isotopic Composition of Water ...... 29 Oxygen-18 and Deuterium ...... 29 Tritium ...... 31 Limitations and Future Needs...... 31 Summary and Conclusions ...... 34 Selected References...... 34

FIGURES 1–3. Maps showing: 1. Location of the Yucaipa area in the Santa Ana River drainage basin, southern California...... 2 2. Physiography of the Yucaipa area, southern California ...... 3 3. Selected wells and surface-water-quality sites in the Yucaipa area, southern California...... 4 4. Graph showing tritium activity in precipitation at Los Angeles, California, 1953–96 ...... 6 5–8. Maps showing: 5. Surficial geology of the Yucaipa area, southern California...... 10 6. Ground-water levels at selected wells in the Yucaipa area, southern California, spring 1997...... 12 7. Land use in the Yucaipa area, southern California, 1990...... 14 8. Water chemistry in samples from selected wells and surface-water sites in the Yucaipa area, southern California ...... 18 9. Trilinear diagrams showing major-ion composition of surface water and ground water in the Yucaipa area, southern California...... 20 10. Map and graphs showing precipitation stations and cumulative precipitation for three February 1998 storms in the Santa Ana River drainage basin, southern California...... 21 11. Boxplots showing concentration of selected constituents for selected wells and surface-water sites in the Yucaipa area, southern California ...... 23 12. Map showing concentration of dissolved solids, nitrites plus nitrates, and dissolved oxygen for selected wells and surface-water sites in the Yucaipa area, southern California...... 24 13. Diagram showing driller’s log, electric logs, vertical flow rate, well construction, and water-quality sampling for well 1S/2W-25R4 in the Yucaipa area, southern California ...... 27

Contents III 14. Graph showing isotopic concentrations of delta deuterium compared to delta oxygen-18 by site and by storm for selected wells and surface-water sites in the Yucaipa area, southern California...... 30 15. Map showing delta deuterium, delta oxygen-18, and tritium activity in selected wells and surface-water sites in the Yucaipa area, southern California ...... 32

TABLES 1. Location and characteristics of selected surface-water sites and wells in the Yucaipa area, southern California .. 13 2. Chemical and isotopic analyses of water from selected surface-water sites in the Yucaipa area, southern California ...... 36 3. Chemical and isotopic analyses of water from selected wells in the Yucaipa area, southern California...... 39

CONVERSION FACTORS, VERTICAL DATUM, ACRONYMS, AND ABBREVIATIONS, AND WELL-NUMBERING SYSTEM

Conversion Factors

Multiply By To obtain cubic foot per second (ft3/s) 0.02832 cubic meter per second foot (ft) .3048 meter foot per year (ft/yr) .3048 meter per year gallon per day per square foot [(gal/d)/ft2] .3516 liter per day per square meter gallon per minute (gal/min) .003785 cubic meter per minute inch (in) 25.4 millimeter inch per year (in/yr) 2.54 centimeter per year mile (mi) 1.609 kilometer

Temperature is given in degrees Celsius (AC), which can be converted to degrees Fahrenheit (AF) by the following equation: AF = 9/5(AC) + 32.

Vertical Datum

Sea level: In this report, “sea level” refers to the National Geodetic Vertical Datum of 1929 (NGVD of 1929)—a geodetic datum derived from a general adjustment of the first-order level nets of both the United States and Canada, formerly called Sea Level Datum of 1929.

Acronyms and Abbreviations mg/L milligrams per liter Hg/L micrograms per liter HS/cm microseimens per centimeter δD delta deuterium δ18O delta oxygen-18 per mil parts per thousand, as used with delta (δ) notation pCi/L picocuries per liter

14C carbon-14 CCYN Carbon Canyon Dam CONV Converse Fire Station DEVO Devore Fire Station GIS geographic information system 3H tritium

IV Contents LKMA Lake Mathews LSD Land-Surface datum relative to NGVD of 1929 MCL maximum contaminant level MTS mountains NO2 nitrite NO3 nitrate OAKG Oak Glen PRDO Prado SAR5 Santa Ana River 5th Street SARM Santa Ana River near Mentone SMCL secondary maximum contaminant level SNTO San Antonio Dam VSMOW Vienna Standard Mean Ocean Water

Well-Numbering System

Wells are identified and numbered according to their location in the rectangular system for the subdivision of public lands. The identification consists of the township number, north or south; the range number, east or west; and the section number. Each section is further divided into sixteen 40- acre tracts lettered consecutively (except I and O), beginning with “A” in the northeast corner of the section and progressing in a sinusoidal manner to “R” in the southeast corner. Within the 40-acre tract, wells are sequentially numbered in the order they are inventoried. The final letter refers to the base line and meridian. In California, there are three base lines and meridians; Humboldt (H), Mount Diablo (M), and San Bernardino (S). All wells in the study area are referenced to the San Bernardino base line and meridian (S). Well numbers consist of 15 characters and follow the format 002S002W02M001S. In this report well numbers are abbreviated and written 2S/2W-2M1. Wells in the same township and range are referred to only by their section designation, 2M1. The following diagram shows how the number for well 2S/2W-2M1 is derived.

RANGE R4W R3W R2W R1W R1E R2W T2N 6 5 4 3 2 1 D C B A

T1N MERIDAN BASE LINE 7 8 9 10 11 12 E F G H T1S 2 18 17 16 15 14 13 M L K J T2S

TOWNSHIP T2S 19 20 21 22 23 24 N P Q R T3S 30 29 28 27 26 25 Well 31 32 33 34 35 36 2S/2W-2M1

Well-numbering diagram

Contents V Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996−98

By Gregory O. Mendez, Wesley R. Danskin, and Carmen A. Burton

ABSTRACT recharged since 1952. The youngest ground water (greater than 7 picocuries per liter) was found near The quality of surface water and ground the hills and mountains surrounding the Yucaipa water in the Yucaipa area was evaluated to deter- area; the oldest ground water (less than mine general chemical characteristics and to iden­ 0.3 picocuries per liter) was found in the Western tify areas of recent ground-water recharge. Water Heights subbasin. samples, collected from 8 sites on 3 creeks and Testing of the vertical contribution of from 25 wells, were analyzed for general chemis­ ground water to well 1S/2W-25R4 showed that try, nutrients, tritium, and stable isotopes of hydro­ more than one-half of the water flowed into the gen and oxygen. At one production well well between depths of about 450 and 600 feet (1S/2W-25R4), water samples were collected at below land surface; the rest of the water flowed discrete depths during pumping and a continuous into the well between 600 and about 850 feet profile of the vertical flow rate inside the well cas­ below land surface. At a discharge rate of ing was recorded. In addition to general-chemistry 750 gallons per minute, virtually no water was samples, tritium and carbon-14 samples were col­ contributed to the well below a depth of about 850 lected at this well to interpret the age of water at feet. The water samples collected at this well different depths. ranged in age from less than 50 to less than 400 Results indicate that most water in the years before present. Yucaipa area is a calcium-bicarbonate type. The general chemical composition of surface water resembles that of ground water, although the con­ INTRODUCTION centration of most constituents is higher in ground water. The chemical composition of most ground- The Yucaipa area is about 12 mi southeast of the water samples is similar. Elevated concentrations city of San Bernardino and about 75 mi east of the city of nitrate in some ground-water samples may indi­ of Los Angeles in the upper part of the Santa Ana River cate recharge from agricultural areas. drainage basin (fig. 1). Since about 1970 and especially In surface water that recharges ground water during the 1990’s, the widespread urbanization of tritium activity ranged from 7 to 18 picocuries per southern California has extended inland from the coast liter. The range of tritium activity found in ground into the Yucaipa area. Undeveloped land, agricultural land, and sparsely populated residential land have been water indicates different times since recharge and converted into housing tracts. The net effect of this possible mixing along ground-water flow paths. change in land use has been an increase in the demand The oldest ground-water sample had a tritium for water, especially potable water for domestic use. activity less than 0.3 picocuries per liter, indicating Because the local supply of both surface water and more than 50 years since recharge. Water samples ground water is limited in this semiarid region, water that had tritium activity greater than 0.3 picocuries purveyors need an accurate assessment of water per liter indicate that some of the water was resources. This report assesses the quality of water in

Introduction 1 the Yucaipa area, primarily in the Yucaipa plain (fig. 2). analysis of these data was used to identify areas of The report will aid local water purveyors in under- recent ground-water recharge and evapotranspiration, standing and evaluating local resources and using them and to determine generalized ground-water flow paths. most effectively in combination with water imported The scope of this study was to collect and ana­ from northern California and from the adjacent San lyze water samples from streams and wells in the Bernardino area. Yucaipa area. All samples were collected during 1996–98 as composite (bulk) samples, which then were Purpose and Scope split into appropriate subsamples for analysis. Previ­ ously collected data, which did not include analysis for The purpose of this study, the results of which tritium or stable isotopes, were not included in this are presented in this report, was to survey the quality of study. Several water samples were collected from the surface water and ground water in the Yucaipa area. surrounding hills and mountains, but the focus of the Water samples collected as part of the study were ana- sampling and subsequent analysis was on water quality lyzed for general chemistry, nutrients, tritium, and sta- of the Yucaipa plain. A sample collected from Mill ble isotopes of hydrogen and oxygen. Preliminary Creek (fig. 3), which originates in the San Bernardino

Figure 1. Location of the Yucaipa area in the Santa Ana River drainage basin, southern California.

2 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Mountains east of Yucaipa, represents ground water Methods of Investigation emanating as springflow from nearby bedrock. This water is imported into the Yucaipa Regional Park and Collection of several areally distributed surface- used to fill recreational lakes, and then recharges the water samples was required to characterize surface- ground water. Six depth-dependent water samples were water quality and to identify the likely interaction collected from a single production well (1S/2W-25R4) between surface water and ground water. Because and were compared to vertical flow rates within the streamflow on the Yucaipa plain is infrequent and of well. A geographic information system (GIS) was short duration, simply finding surface water to sample developed to locate wells, to aid in interpretation of can be difficult in this semiarid region. Fortuitously, the water-quality data, and to prepare figures for this winter of 1997–98 was an El Niño year with greater report. than average runoff. Three storms in February 1998

Figure 2. Physiography of the Yucaipa area, southern California.

Introduction 3 Figure 3. Selected wells and surface-water-quality sites in the Yucaipa area, southern California.

4 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Figure 3—Continued.

Introduction 5 were selected to collect water samples. Streamflow was The strategy for sampling ground water was to sampled on Oak Glen and Yucaipa Creeks, which are collect samples throughout the Yucaipa area to identify the two primary streams in the area (fig. 3). Base-flow the general quality, the likely source of recharge, and samples were collected on upper Oak Glen Creek in the the dominant paths of ground-water flow. Nearly all foothills, where flow is present and originates as ground-water samples were obtained as bulk samples springflow from bedrock or as snowmelt. Yucaipa from discharge pipes of production wells. At a new pro- Creek originates in the southern part of the Yucaipa duction well (1S/2W-25R4), it was possible to obtain depth-dependent samples under pumped conditions Hills and has no base flow. One water sample was col- using a sampling technique described by Izbicki and lected from Mill Creek because part of its flow is others (1999). Coincident with sampling, the flow rate pumped into the Yucaipa area in a pipeline and then is inside the casing of the production well was measured discharged at the Yucaipa Regional Park. The imported using a spinner tool. Flow-rate measurements were water is used for recreational purposes before it infil- used to determine the relative contributions of ground trates into the ground. Water in the pipeline is a mixture water from different strata to the pumped well. of streamflow diverted in the upper Mill Creek drainage In this study, naturally occurring stable isotopes basin and streamflow diverted under Highway 38 (fig. of oxygen (oxygen-18) and hydrogen (deuterium) were 3). Water from Mill Creek was collected as a single used to help determine the source of ground water and grab sample; other surface-water samples were col- to trace its movement. Atoms of oxygen-18 and deute­ lected, depending on the stream conditions, as either an rium have more neutrons and a greater atomic mass equal-width integrated sample or a grab sample. (weight) than do the more common isotopes,

2,250 700

2,000 600

1,750

500 1,500

1,250 400

1,000 300

750 Volume-weighted tritium 200

500 Decay-corrected to 1996 TRITIUM ACTIVITY, IN UNITS (TU)

TRITIUM ACTIVITY, IN PICOCURIES PER LITER 100 250

0 0 1950 1955 1960 1965 1970 1975 1980 1985 1990 1995 2000 YEAR

Figure 4. Tritium activity in precipitation at Los Angeles, California, 1953–96. Tritium was corrected using techniques from Michel (1989).

6 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 oxygen-16 and hydrogen. This difference in weight lated using techniques described by Michel (1989), results in differences in the physical and chemical (fig. 4). Because tritium can be part of the water mole­ behavior of the heavier, less abundant isotopes (Inter- cule, tritium is not affected by reactions other than national Atomic Energy Agency, 1981). radioactive decay; therefore, tritium is an excellent Most of the world’s precipitation originates from tracer of the movement of water on time scales ranging the evaporation of seawater. As a result, the oxygen-18 from 10 to about 50 years before present. Ground water and deuterium composition of precipitation throughout having tritium activities less than the detection limit of the world is linearly correlated and often referred to on 0.3 pCi/L is considered to have been recharged before graphs as the meteoric water line (Craig, 1961). 1952. Ground water having measurable tritium activity Oxygen-18 and deuterium abundances typically are is considered to be recharged after 1952. 14 expressed as ratios in delta notation (δ), as per mil Carbon-14 ( C) is a naturally occurring radioac­ (parts per thousand) differences, relative to the stan­ tive isotope of carbon that has a half-life of about 5,730 dard known as Vienna Standard Mean Ocean Water years. Carbon-14 data are expressed as percent modern 14 (VSMOW) (Gonfiantini, 1978). By convention, the carbon by comparing C activities to the specific activ­ value of VSMOW is 0 per mil. Oxygen-18 and deute­ ity of National Bureau of Standards oxalic acid (12.88 rium ratios relative to VSMOW can be measured more disintegrations per minute per gram of carbon in 1950 precisely than absolute abundances. Analytical preci­ equals 100 percent modern carbon). 14 sion is generally within 0.05 per mil for δ18O (delta Carbon-14 is not part of the water molecule and C oxygen-18) and within 1.5 per mil for δD (delta deute­ activities can be affected by chemical reactions rium) (Izbicki, 1996). between dissolved constituents and aquifer material. Water that condenses at cooler temperatures Carbon-14 is a tracer of the movement and relative age (typically associated with higher altitudes, cooler of water on time scales ranging from several hundred to climatic regimes, or higher latitudes) is lighter (more more than 20,000 years before present. negative) than water that condenses at warmer temper­ Field parameters such as specific electrical con­ atures (typically associated with lower altitudes, ductance, pH, and dissolved oxygen were measured for warmer climatic regimes, or lower latitudes). In addi­ both surface-water and ground-water samples in the tion, water that has been partly evaporated is enriched field using probes calibrated with appropriate stan­ by fractionation of the heavier isotopes relative to its dards. Alkalinity was determined in the field by titra­ tion with a dilute sulfuric acid. All field measurements original composition. On graphs of δ18O and δD, partly evaporated water samples plot to the right of the mete­ were made in accordance with the National Field Man­ oric water line along a line known as the evaporative ual for the Collection of Water-Quality Data (Wilde and Radtke, 1998). The techniques used for the collec­ trend line. As a result, the δ18O and δD composition of tion and processing of inorganic constituents were a water sample can provide a record of the source and made in accordance with Horowitz and others (1994). evaporative history of the water. Analyses for inorganic constituents were done by the Tritium and carbon-14 samples were collected to 3 U.S. Geological Survey National Water Quality Labo­ help identify the age of water. Tritium ( H) is a natu­ ratory using techniques described by Fishman and rally occurring radioactive isotope of hydrogen that has Friedman (1989), Fishman (1993), Patton and Truitt a half-life of about 12.4 years. In this study, the activity (1992), and Struzeski and others (1996). of tritium was measured in picocuries per liter (pCi/L); 1 pCi/L is equivalent to about 2.2 disintegrations of tri­ tium per minute or about one tritium atom in Previous Investigations 3.1 Z 1017 atoms of hydrogen. Prior to 1952, tritium activity in precipitation in coastal southern California Many investigations have been made since the was about 6 pCi/L. As a result of atmospheric testing of early 1900’s in the upper Santa Ana River drainage nuclear weapons from 1952 to 1962, tritium activity basin and, in particular, in the adjacent San Bernardino increased to greater than 2,000 pCi/L (Michel, 1976). area (fig. 2). Several previous investigators have Tritium concentrations and decay-corrected values in included parts of the Yucaipa area on the periphery of precipitation at Los Angeles, California, were calcu­ their study, but most have described only generalized

Introduction 7 data and concepts for the Yucaipa area. Such general­ individuals in the Yucaipa area—in particular, Joseph ized information includes description of the regional B. Zoba, John “Jack” Nelson, Brent J. Anton, and hydrology (Mendenhall, 1905), estimation of ground- Frank E. Jubula with the Yucaipa Valley Water District; water-storage capacity (Eckis, 1934), calculation of E. Bernice Long, previously with the Western Heights ground-water outflow from the Yucaipa area (Dutcher Water District; and Michael L. Huffstutler, previously and Burnham, 1959; Burnham and Dutcher, 1960), with the City of Redlands—who greatly aided us in depiction of ground-water levels and susceptibility of obtaining and understanding field data. We thank U.S. liquefaction during a major earthquake (Matti and Geological Survey colleagues Jonathan C. Matti for Carson, 1991), and evaluation of regional water- providing geologic map data and Kelly R. McPherson management options (California Department of Water for creating a geographical information system that Resources, 1970, 1979, 1986). aided in analysis of data and preparation of map fig­ The more detailed investigations in the Yucaipa ures. We also thank the several individuals who helped area have focused on surficial geology and ground- review and prepare the report, including Alan Welch water quantity. Surficial geology of the area has been (review), Jim Bowers (review), Larry G. Schneider mapped at a scale of 1:48,000 by Morton (1974) and (illustrations), Jerrald A. Woodcox (editing), and James more recently at a scale of 1:24,000 by Matti and others B. Baker (layout and publication). (1992). A detailed calculation of ground-water outflow from the area south of the Crafton Hills was made by Dutcher and Fenzel (1972). Sustainable yield of the DESCRIPTION OF STUDY AREA ground-water basin was calculated by Mann (1986) and later by Todd (1988), and an explanation of the dif­ ferences between the two yield calculations was made Physiography by Mann and Todd (1990). The potential for artificial recharge was evaluated by Moreland (1970). Changes The study area is bordered on the west by the in ground-water levels were summarized by Fletcher Crafton Hills, on the east by the Yucaipa Hills, on the (1976) and Fox (1987), and a plan to monitor ground- north by the San Bernardino Mountains, and on the water levels for much of the Yucaipa area was proposed south by the badlands (fig. 2). Between the hills and by Fox (1990). A ground-water-flow model was devel­ mountains is a gently sloping area of unconsolidated oped for the upper part of the Oak Glen Creek drainage deposits, commonly referred to as the Yucaipa plain or by Powers and Hardt (1974). Water-management plans the Yucaipa ground-water basin. On the northwest side, were prepared for the Western Heights Water District the plain merges into the San Bernardino valley, and on (Egan and Associates, Inc., 1989) and for the Yucaipa the southeast side, the plain opens to the San Gorgonio Valley Water District (Camp, Dresser, and McKee, Pass. The Yucaipa plain ranges in altitude from about 1994). 1,800 to 3,600 ft above sea level. The hills and moun­ Measurements of surface-water discharge in the tains surrounding the plain range in altitude from about Yucaipa area are scant. A much greater number of 3,000 ft in the Crafton Hills, to 5,000 ft along the ridge ground-water-level measurements are available for of the Yucapia Hills, to more than 8,000 ft in the San many wells in the area, including historical data that Bernardino Mountains. span several decades. Measurements of water quality for both surface water and ground water are made rou­ tinely to ensure that drinking-water standards are met. Population and Climate Other measurements of water chemistry, such as isoto­ pic concentrations of hydrogen and oxygen, had not The study area includes parts of San Bernardino been made prior to this study. and Riverside Counties and the major cities of Yucaipa and Calimesa (fig. 3). In 1998, the population in the Yucaipa study area was about 38,200. Most residents in Acknowledgments the area live on the plain, but many live in the surround­ ing foothills. Recent residential development is con­ The authors thank the San Bernardino Valley centrated on the east side of Crafton Hills, on the Municipal Water District for providing cooperative Yucaipa Hills, and along the lower altitudes of the San funding for this project. Also, we thank several Bernardino Mountains.

8 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Climate in the study area is moderate with long, to well-consolidated deposits has resulted in deeply dry summers and short, wet winters. On the plain, sum­ incised streambeds such as the channels of Oak Glen mer temperatures range from about 60 to 100 oF and and Yucaipa Creeks. Isolated deposits of slightly con­ winter temperatures range from about 40 to 70 oF. solidated younger alluvium border parts of the stream Annual precipitation in this semiarid region averages channels and badlands. Unconsolidated recent allu­ about 18 in/yr on the plain, and as much as 40 in/yr in vium is present in stream channels throughout the the San Bernardino Mountains (Todd, 1988). Precipita­ Yucaipa plain and has its greatest width in the Western tion falls almost exclusively as rain on the plain; snow Heights subbasin. is the predominant precipitation above an altitude of The geologic structure and landforms in the about 6,000 ft. Snowpack in the San Bernardino Moun­ Yucaipa area are mostly a result of regional tectonism. tains commonly lasts into April and, occasionally, May. To the north, the San Andreas Fault separates two tec­ tonic plates—the North American Plate on the east and the Pacific Plate on the west (Harden, 1998, fig. 1–4). Geology In addition to creating the sediment-filled graben that forms the Yucaipa ground-water basin, the structural Bedrock, which forms the hills and mountains forces associated with plate tectonics have caused sev­ that surround the Yucaipa plain on the north, east, and eral additional faults, some of which are visible at the west sides, is composed mostly of crystalline igneous land surface. One set of visible faults is subparallel to and metamorphic rocks of Cenozoic to Mesozoic age the northwest-trending San Andreas and San Jacinto (fig. 5). These basement rocks consist predominantly of Faults and includes the Banning and Oak Glen Faults; granodiorite, although granite, quartz monzonite, another set is nearly perpendicular to the first and tonalite, dioritic gneiss, and schist also are present includes the Chicken Hill Fault (fig. 5). Numerous (Matti and others, 1992). Basement rocks in the additional barriers, which are hypothesized to be faults, Yucaipa Hills are cataclastically deformed and contain have been inferred by geophysical and ground-water- abundant fractures and intruded quartz veins. Some level data. sedimentary rocks, mostly sandstone, mantle part of the crystalline bedrock in the vicinity of Mill Creek. The badlands to the south consist of poorly to moder­ Hydrology ately consolidated continental deposits of Pleistocene and Pliocene age that have been uplifted and dissected. The Yucaipa area is within the upper part of the In the badlands, the deposits consist of alternating beds Santa Ana River drainage basin and encompasses much or lenses of gray, yellow, or brown gravel, sand, silt, of the San Timoteo Creek drainage (figs. 1 and 2). and clay. The gravel is predominantly from granitic Although surface-water drainage is well defined to the rocks but contains numerous fragments of metamor­ north in the San Bernardino Mountains, the drainage phic and volcanic rocks. These badland deposits are cut becomes progressively less defined to the south in the by numerous faults and in places are gently to intensely more extensively eroded badlands. The Yucaipa area is folded. drained by three primary streams: Wilson and Oak Between the San Bernardino Mountains and the Glen Creeks, which flow from the San Bernardino badlands is a down-dropped block of crystalline rocks Mountains, and Yucaipa Creek, which flows from the bounded on either side by the San Andreas Fault and Yucaipa Hills (fig. 3). These streams coalesce and flow the San Jacinto Fault (fig. 2). Erosion of the hills and into San Timoteo Creek, which exits the area to the mountains that surround the Yucaipa area has filled this southwest (fig. 2). tectonically created trough, called a graben, with allu­ The semiarid conditions in the Yucaipa area limit vial deposits that are as much as 1,500 ft thick. The the quantity and frequency of streamflow. Generally, alluvial deposits are composed of several units ranging streamflow is present in the middle and lower reaches in age from late Pleistocene (very old alluvium) to of Wilson, Oak Glen, and Yucaipa Creeks only for brief Holocene age (recent alluvium) (fig. 5). The very old or periods after rain. Flow in the upper reaches of Oak older alluvium unconformably overlies most of the Glen Creek is perennial as a result of ground-water dis­ basement rocks. These alluvial deposits are both of late charge from Ford Canyon in the San Bernardino Moun­ Pleistocene age and consist of boulders, gravel, sand, tains (fig. 3). Some of this flow is diverted for public silt, and clay. Subsequent erosion of these moderately supply. Just upstream from the Casa Blanca Barrier

Description of Study Area 9 Figure 5. Surficial geology of the Yucaipa area, southern California.

10 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 (fig. 5), streamflow infiltrates into the unconsolidated water is more complex. Faults in the area divide the deposits of the Yucaipa plain. In some places, flow in ground-water basin into several subbasins (Moreland, San Timoteo Creek is now perennial as a result of agri­ 1970), which previous investigators have characterized cultural and urban runoff. as being relatively isolated from one another (fig. 6). The unconsolidated deposits of the Yucaipa Flow in and between subbasins is complex and is not plain—the recent, younger, older, and very old allu­ well understood except as can be inferred from contour vium (fig. 5)—constitute the primary source of ground maps of ground-water levels (Moreland, 1970, figs. water in the area and together compose the valley-fill 6–8; Todd, 1988, fig. 11). This lack of understanding of aquifer. Permeability of these deposits ranges from 50 ground-water movement was a major impetus for this to 300 (gal/d)/ft2 (Burnham and Dutcher, 1960, p. 80). water-quality study, in particular for the collection of Recent river-channel deposits, especially near the hills isotopic data. and mountains, appear to be unweathered and very per­ Detailed ground-water-level maps for different meable, but most are above the water table. Most time periods, possibly corroborated by results from a ground water occurs in the older, moderately consoli­ ground-water flow model, are needed to better under- dated alluvium at minimum depths of about 200 ft stand the flow between subbasins and to help interpret below land surface. Although the base of the valley-fill water-quality data. As a starting point, however, aquifer is unknown, it probably is more than 1,500 ft ground-water-level data from spring 1997 were below land surface in most parts of the Yucaipa plain. obtained from local water agencies (fig. 6 and table 1). In the western part of the plain, ground water histori­ On the basis of these data and ground-water-level maps cally was under artesian conditions, which may indi­ from Moreland (1970), ground water in the cate the presence of fine-grained material of lower Triple Falls Creek subbasin (fig. 6) appears to flow permeability within the valley-fill aquifer. from the east to the west toward the north end of For the most part, the crystalline rocks of the sur­ Crafton Hills. In the Wilson Creek and Crafton subba­ rounding hills and mountains and underlying the sins, ground water flows generally from north to south. valley-fill aquifer are poorly permeable. However, the In the Calimesa subbasin, ground water flows from east multi-directional tectonic forces in the Yucaipa area to west, toward the San Bernardino area. Insufficient have created highly fractured, cataclastic rock, which data were available in the Western Heights subbasin to in some places is moderately permeable. Some wells, determine the direction of ground-water flow, but in the including large municipal wells, have been completed past (1930–70), a pumping depression was present near in the crystalline rocks in order to increase well yield. Dunlap Acres (Moreland, 1970). Faults are important not only because of their influence on the general topography, but also because Land Use of their influence on the flow of ground water. Fault zones in consolidated rocks commonly consist of fis­ Originally, the Yucaipa area was inhabited by sures that may serve as conduits for ground-water flow. Native Americans, and the name “Yucaipa” is derived Conversely, faults that transect permeable unconsoli­ from the Serrano Indian word “Ucipe,” which means dated materials may produce barriers to ground-water wet and sandy. Until the early 1800’s, the area was flow. For example, the San Andreas Fault along the under Spanish rule as part of the San Bernardino Ran­ base of the San Bernardino Mountains is known to be a cho. By 1860, the land was privately owned by a few barrier to ground-water flow because its trace in the families. In the early 1900’s, part of the area was sub- alluvium at the mouth of nearly every canyon is marked divided into apple orchards, and the area became syn­ by springs and dense vegetation. Although the barrier onymous with red apples. effects displayed by faults are not completely under- After 1940, the Yucaipa area became extremely stood, the presence of offset beds, gouge material, popular as a retirement destination. Many mobile- sharp folds, and chemical cementation are suspected to home parks were built, mostly along the upper part of contribute to reduced permeability. the Yucaipa plain near the San Bernardino Mountains. On a basinwide scale, the general movement of Rural-type residential development continued to be both surface water and ground water is southward and popular and covered much of the central part of the westward from the surrounding hills and mountains. Yucaipa plain. As more of the area was urbanized, cul­ On a local scale, however, the movement of ground tivation of citrus was moved to the edges of the plain,

Description of Study Area 11 Figure 6. Ground-water levels at selected wells in the Yucaipa area, southern California, spring 1997.

12 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Table Location and characteristics of selected surface-water sites and wells in the Yucaipa area, southern California. [YVWD, Yucaipa Valley Water District; WHWD, Western Heights Water District; SMWD, South Mesa Water District; LSD, land-surface datum; ft, foot; na, not applicable; —, no data] Altitude of water Altitude Open intervals Other well table Depth of well Site name or State well number Well owner Latitude Longitude of LSD below LSD identifiers (ft above (ft) (ft) (ft) sea level)1 Upper Oak Glen Creek in Ford Canyon na na 340326 1165605 5,920 na na na Oak Glen Creek in Ford Canyon na na 340320 1165612 5,560 na na na Oak Glen Creek near Oak Glen na na 340307 1165621 3,550 na na na Oak Glen Creek at 2nd street na na 340238 1170232 2,620 na na na Yucaipa Creek at Mesa Grande Bridge na na 340051 1170026 2,880 na na na Yucaipa Creek at 5th street na na 340049 1170314 2,390 na na na Yucaipa Creek below Dunlap Acres na na 340037 1170643 1,880 na na na Mill Creek at Yucaipa Regional Park na na 340316 1170251 2,630 na na na 1S/1W-19G1 YVWD YVWD # 31 340415 1170127 3,086 2,883 384 — 1S/1W-27L1 YVWD YVWD # 25 340312 1165839 3,875 — 30 15–30 1S/1W-32C1 YVWD YVWD # 13 340253 1170027 3,194 3,177 307 26–415 1S/2W-24C2 YVWD YVWD # 51 340438 1170242 2,695 2,610 610 230–590 1S/2W-25A1 YVWD YVWD # 37 340343 1170212 2,780 2,584 305 — 1S/2W-25R4 YVWD YVWD # 53 340255 1170216 2,730 2,458 970 450–950 1S/2W-34N1 City of Redlands — 340202 1170502 2,157 1,790 — — 1S/2W-36G1 YVWD YVWD # 46 340236 1170231 2,623 — 1,150 340–1,140 2S/1W-08F1 YVWD YVWD # 27 340054 1170029 2,878 2,819 314 164–314 2S/1W-15F2 YVWD YVWD # 61 340003 1165825 3,515 — 462 189–462 2S/2W-01J1 YVWD YVWD # 50 340124 1170213 2,600 2,284 352 330–350 2S/2W-02M1 YVWD YVWD # 11 340129 1170351 2,401 2,141 525 260–450; 465–525 2S/2W-03E1 WHWD WHWD # 6 340148 1170454 2,170 1,794 599 135–578 2S/2W-03L1 City of Redlands Chicken Hill 340129 1170442 2,200 2,096 505 198–485 2S/2W-04G3 WHWD WHWD # 2A 340144 1170536 2,100 1,779 630 400–620 2S/2W-04G4 WHWD WHWD # 11 340137 1170535 2,080 — 1,690 705–1,205; 1,210–1,690 2S/2W-04J2 WHWD WHWD # 5A 340135 1170516 2,095 1,773 1,100 390–1,090 2S/2W-04R1 WHWD WHWD # 9 340120 1170513 2,091 1,753 600 150–576 Description ofStudy Area 2S/2W-10B2 City of Redlands Hog Canyon #2 340106 1170450 2,180 2,105 700 260–440; 460–680 2S/2W-11A1 YVWD YVWD # 24 340105 1170316 2,446 2,146 585 320–585 2S/2W-11D1 YVWD YVWD # 10 340057 1170406 2,327 2,129 515 170–500 2S/2W-14C1 SMWD SMWD # 2 340014 1170343 2,393 2,167 363 205–363 2S/2W-14R3 SMWD SMWD # 4 335924 1170317 2,340 — 1,000 352–976 2S/2W-24L1 YVWD YVWD # 48 335848 1170243 2,327 — 1,180 380–870; 930–1,160 2S/2W-28C2 Fisherman's Retreat — 335829 1170552 1,943 — — — 1 13 Altitude of water levels provided by water districts for spring 1997. Figure 7. Land use in the Yucaipa area, southern California, 1990.

14 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Figure 7—Continued.

Description of Study Area 15 and since about 1990, most of the citrus groves have increased pumpage and reduced recharge caused by been replaced with planned residential developments. below-normal precipitation resulted in an increased As of 1990, land use in the Yucaipa area was a rate of decline in ground-water levels of 10 to 20 ft/yr. combination of residential land covering much of the This rate continued into the early 1960's and then Yucaipa plain, and isolated pieces of agricultural land decreased to 5 to 10 ft/yr (Moreland, 1970). Because (fig. 7). The central part of the plain continues to be population predictions indicate that local water needs filled with small, older homes occupying as much as an will increase sharply over the next decade, it is likely acre of land. Mobile-home parks continue in their same that ground-water levels will continue to decline in location along the northern part of the plain. Recently some parts of the Yucaipa area. constructed tract housing, at densities of 1 to 6 homes per acre, extends to the edges of the plain and onto the surrounding hills. Within the boundaries of the Yucaipa WATER QUALITY Valley Water District, which covers most of the plain, rural residential housing (less than or equal to 1 dwell­ Water samples were collected from selected sur­ ing unit per acre) accounts for 35 percent of the land face-water sites and wells in the Yucaipa area during use, low-density residential housing (1 to 4 dwelling 1996–98. These sites and wells are shown in figure 3 units per acre) accounts for 21 percent, and planned and listed in table 1. Results of chemical analyses of 15 residential development (mixed residential, public surface-water samples from 8 sites on 3 creeks and of land, and some commercial use) accounts for 32 ground-water samples from 25 wells are given in 29 percent (Camp, Dresser, and McKee, 1994). tables 2 and 3, respectively, in the back of this report. The small amount of commercial development in On the basis of these data, the major-ion composition the Yucaipa area is located along a few main streets, of water was evaluated using Stiff (polygon) and Piper and there is almost no industrial development. Apple (trilinear) diagrams (figs. 8 and 9). A Stiff diagram growing is still popular on the lower slopes of the San shows the relative abundance of cations and anions Bernardino Mountains, particularly along Oak Glen expressed in milliequivalents per liter and plotted on Creek, and each fall many visitors attend the apple har­ one of four parallel horizontal axes (Stiff, 1951). The vest festival. The Yucaipa Regional Park, with its small resulting polygon shows similarities or differences in lakes and grassy areas, is located on the northwest side general water chemistry, and the width of the polygon of the Yucaipa plain adjacent to Crafton Hills. The is an approximation of the total ionic content. A Piper small lakes are sustained by water imported from Mill diagram (Piper, 1944) shows the relative contribution Creek. On Wilson Creek, a large artificial-recharge of major cations and anions, on a charge-equivalent basin has been constructed and can be used to recharge basis, to the total ionic content of the water. Percentage both local runoff and water imported from Mill Creek. scales along the sides of the diagram indicate the rela­ tive concentrations, in milliequivalents per liter, of each major ion. Cations are shown in the left triangle, anions Water Use are shown in the right triangle, and the central diamond integrates the data. Prior to the late 1800’s, the water supply of the Yucaipa area was limited to surface flow in the moun­ tain streams and small quantities of springflow along Surface Water the Chicken Hill Fault. In the 1890's and early 1900's, a number of flowing wells were completed in the West- Oak Glen, Yucaipa, and Mill Creeks were ern Heights subbasin. At that time, several water com­ selected for the collection of water-quality samples. panies were formed to distribute water for irrigation. Four sites were located on Oak Glen Creek, in down- Agricultural development during the period 1900–30 stream order: two sites in Ford Canyon, one site near required the installation of more wells throughout the the town of Oak Glen, and one site at the Second Street area. By the 1930’s, this increased pumping had low­ crossing, just downstream from the confluence with ered the hydraulic head in the valley-fill aquifer to Wilson Creek. Three sites were chosen on Yucaipa below land surface. This gradual decline in ground- Creek, in downstream order: at the Mesa Grande water levels continued until the post-World War II bridge, at the Fifth Street bridge, and southwest of development boom began in 1945. A combination of Dunlap Acres downstream from the confluence with

16 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Oak Glen Creek (fig. 3). One sample was collected at except at the Devore Fire Station (DEVO) and San Yucaipa Regional Park where water from Mill Creek is Antonio Dam (SNTO) stations, both of which recorded imported to the park in a pipeline. The water in the nearly constant rainfall (fig. 10). The first rain fell in the pipeline originates as diversions from two locations on afternoon of February 22, and the rest fell in the early Mill Creek. The upper diversion is located in the evening of February 23. The precipitation was greatest incised drainage channel and is used as inflow to a in the mountains to the north: 6.3 in. at DEVO; 5.2 in. powerhouse; the lower diversion is under the Highway at SNTO; and 4.5 in. at OAKG. The precipitation was 38 bridge (fig. 3). least, about 1.9 in., in the southern part of the basin at The winter of 1997–98 was much wetter than the Santa Ana River at Fifth Street (SAR5) and at Lake average because of El Niño conditions. This weather Mathews (LKMA). pattern is caused by warming of the tropical Pacific Storm runoff flows quickly out of the surround­ Ocean and can result in extreme weather throughout ing hills and mountains onto the plain with little time the world and greater than average precipitation in for the water to dissolve minerals and salts. As a result, southern California. As a result of El Niño conditions, water-quality samples from Yucaipa Creek had very February 1998 was the wettest February on record in low concentrations of dissolved solids, cations, and southern California. Late-season storms typically come anions. At the two upstream sites, the concentration of from the Pacific northwest, but also may result from dissolved solids (residue on evaporation) ranged from warm, moist air drawn into southern California from 40 to 57 mg/L (milligrams per liter) (table 2, at back of the southwest. This latter effect produces many of the report). Calcium and bicarbonate, although low in con­ larger magnitude and longer duration storms. centration, were the dominant ions on the basis of mil­ Storms differ in magnitude, duration, intensity, liequivalents (fig. 8). and direction—each of which may produce changes in The chemistry of Oak Glen Creek and Yucaipa water chemistry. In February 1998, three storms were Creek was similar in that water samples were domi­ sampled. From the many precipitation stations in the nated by calcium and bicarbonate ions. However, con­ Santa Ana River drainage basin, nine were chosen to centrations of sodium, magnesium, and sulfate were show storm patterns (fig. 10). The first storm entered higher in samples from Oak Glen Creek. (fig. 8, table the basin from the west and started producing rain at 2). Dissolved-solids concentrations also were higher in Carbon Canyon Dam (CCYN). The rain started falling Oak Glen Creek, ranging from 74 to 249 mg/L (table at about 0700 (local time) on February 3, was basin- 2). The higher concentrations of these constituents may wide in about 6 hours, and lasted about 16 hours. The result simply from the source of the water. Oak Glen greatest precipitation, 2.3 in., was recorded at Prado Creek has its source in the San Bernardino Mountains Dam (PRDO). The least precipitation, about 0.5 in., fell and is perennial in the foothills, whereas the source for at higher altitudes in the mountains to the northeast of Yucaipa Creek is in the Yucaipa Hills. Samples col­ the study area at Converse Fire Station (CONV). Lower lected during base flow in Oak Glen Creek near Oak altitudes to the north and east of Yucaipa received Glen contained higher concentrations of ions than sam­ approximately 2.0 in. of rain, as recorded at the Oak ples collected during stormflows (fig. 8). Calcium Glen station (OAKG). concentrations ranged from 24 to 45 mg/L in base-flow The second storm was the smallest and entered samples, and from 13 to 30 mg/L in stormflow samples. the basin from the west and then moved eastward. Rain Dissolved-solids concentrations ranged from 120 to began falling in the western end of the Santa Ana River 249 mg/L during base flows, and from 74 to 227 mg/L drainage basin during the morning of February 19 and during stormflows. Concentrations of other major ions moved into the rest of the basin starting at about 2000. also decreased during stormflows (fig. 8, table 2). This The greatest precipitation, 0.8 in., was recorded at decrease in concentrations probably results from dilu­ OAKG; the least was 0.1 in. at CONV. tion of base flow with stormflow having a lower ionic The third storm was the largest and started in the strength. mountains to the north. This storm is typical of an El The highest concentration of major ions in Niño-influenced storm whereby tropical moisture from Yucaipa Creek was found at the downstream site, the southwest is entrained in a slow-moving, low- located below the confluence with Oak Glen Creek pressure system moving in from the northwest. The where the surface water exits the study area southwest precipitation generally fell in two distinct periods( of Dunlap Acres (figs. 8 and 9A). The dissolved-solids

Water Quality 17 Figure 8. Water chemistry in samples from selected wells and surface-water sites in the Yucaipa area, southern California.

18 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Figure 8—Continued.

Water Quality 19 100

100

CALCIUM 80 80

60 60 PLUS

40 MAGNESIUM Below� 40 Dunlap� 20 Acres 20 SULFATE PLUS CHLORIDE

0 0 0 0

20 20 0 0 100 SODIUM 40 100 40 20

20 80 60 80 60 PLUS 40 SULFATE BICARBONATE 40 60 80 60 POTASSIUM 80 60

MAGNESIUM 60 40 100 40 80 Below� 100 80 Dunlap� 20 20 CARBONATE100 PLUS Acres

100 0 100 80 60 40 20 0 0 0 20 40 60 80 100 CALCIUM CHLORIDE, FLUORIDE, NO2 + NO3 PERCENTAGE OF TOTAL MILLIEQUIVALENTS PER LITER EXPLANATION Oak Glen Creek - Base flow Mill Creek - Base flow A Oak Glen Creek - Stormflow Yucaipa Creek - Stormflow

100

100

CALCIUM 80 80

60 60 PLUS

40 MAGNESIUM 40 15F2 20 20 SULFATE PLUS CHLORIDE

0 0 0 0 1J1

20 20 28C2 0 100 0 SODIUM 24L1 40 100 40 20

20 80 60 80 60 PLUS 14R3 40 SULFATE BICARBONATE 40 1J1 60 80 60 POTASSIUM 80 60

MAGNESIUM 60 40 100 40 80 15F2 100 20 80 20 28C2 CARBONATE PLUS 24L1 100 100 0 100 80 60 40 20 0 0 0 20 40 60 80 100 CALCIUM CHLORIDE, FLUORIDE, NO2 + NO3 PERCENTAGE OF TOTAL MILLIEQUIVALENTS PER LITER EXPLANATION B 28C2 Abbreviated State well number

Figure 9. Major-ion composition of (A) surface water and (B) ground water in the Yucaipa area, southern California.

20 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 118A00' 117A30' 117A00' 116A30'

0 10 20 MILES 3 (6.3)

0 10 20 KILOMETERS 34A 15' Precipitation station Big Bear� DEVO Lake SNTO SARM CONV Santa Ana River� drainage basin OAKG River Yucaipa� Ana CCYN study� area T e m cinto Ja Ri PRDO e LKMA ve s r c n a a (2.35) l S 1 W a 33A s h 2 (0.8) 45' SAR5 Lake� Santa Elsinore

Pacific� Ocean

3.0 6.0 (6.3) First storm Sample period Third storm 2.5 5.0 Sample period

2.0 4.0

1.5 3.0

1.0 2.0

0.5 1.0

0.0 0.0 Feb 2 Feb 3 Feb 4 Feb 22 Feb 23 Feb 24 1.0 DATE Second storm Sample period EXPLANATION 0.8 Storm plots Station identifier and name

0.6 CCYN: Carbon Canyon Dam CONV: Converse Fire Station DEVO: Devore Fire Station CUMULATIVE PRECIPITATION, IN INCHES LKMA: Lake Mathews near Corona 0.4 OAKG: Oak Glen PRDO: Prado Dam SAR5: Santa Ana River (5th Street) 0.2 SARM: Santa Ana River near Mentone SNTO: San Antonio Dam

0.0 Feb18 Feb19 Feb 20 DATE

Figure 10. Precipitation stations and cumulative precipitation for three February 1998 storms in the Santa Ana River drainage basin, southern California (note change in vertical scale on graphs). Arrows on map show direction storm started in basin; numbers indicate storm sequence sampled and largest amount of total precipitation, in inches. Precipitation data from U.S. Army Corps of Engineers (Gregory Peacock, written commun., 1998). Water Quality 21 concentration was slightly greater than 100 mg/L (table concentrations were low, ranging from 0.18 to 2). The Piper (trilinear) diagram for this surface-water 2.3 mg/L as nitrogen. These low values indicate the sample shows that the dominant ions were mostly cal­ lack of a significant source of nitrate from runoff under cium and bicarbonate (fig. 9A). In comparison with the these conditions. The higher values of nitrate were two upstream sites, this site had a much higher concen­ found in samples collected downstream from the agri­ tration of sulfate (22 mg/L compared to <3.2 mg/L) and cultural land adjacent to Oak Glen Creek and Yucaipa a slightly higher concentration of chloride. The large Creek (figs. 7 and 12). Organic ammonia values ranged differences in the concentrations of many constituents from less than the detection limit of 0.1 mg/L to between the two upstream sites on Yucaipa Creek and 0.7 mg/L. More studies are needed to evaluate the rates the downstream site may be a result of runoff from Oak at which species are converted to and from nitrate. Glen Creek and the town of Yucaipa, or the differences Calcium concentrations ranged from 5.8 to may result from the larger discharge at the time of sam­ 45 mg/L. Chloride and fluoride concentrations ranged pling of the downstream site (190 ft3/s in comparison to from 1.2 to 7.7 mg/L, and from 0.1 to 0.8 mg/L, respec­ 2.3 ft3/s). The sample taken at the downstream site was tively. Sulfate concentrations ranged from 1.4 to collected during the rising limb of the runoff which 37 mg/L. Sodium concentrations ranged from 2.2 to typically carries more sediment. 15 mg/L. Iron and manganese concentrations ranged As found in samples collected from Oak Glen from less than the detection limit of 3 Hg/L to Creek and Yucaipa Creek, the dominant ions in the 110 Hg/L, and from less than the detection limit of sample collected from Mill Creek at the inlet to the 1 Hg/L to 15 Hg/L, respectively. Boron concentrations Yucaipa Regional Park (site H) were calcium and bicar­ ranged from 7 to 24 Hg/L. Barium concentrations bonate (fig. 8). Most constituent concentrations, such ranged from 4.3 to 20 Hg/L. All constituents were well as sodium, chloride, silica, phosphate, boron, and iron, below their respective maximum contaminant levels were similar to concentrations in base-flow samples (MCL) (U.S. Environmental Protection Agency, 1994). collected from Oak Glen Creek at site A and B in Ford Concentrations of dissolved oxygen in samples Canyon (fig. 8 and table 2). These similarities would be collected during the summer from Mill and Oak Glen expected because the source of the water in both creeks Creeks were 8.2 and 8.5 mg/L, respectively. Dissolved- is the San Bernardino Mountains. Other constituents, oxygen concentrations in winter samples from Oak such as calcium, magnesium, dissolved solids, and sul­ Glen and Yucaipa Creeks ranged from 9.4 to fate, had concentrations similar to those in stormflow 10.8 mg/L. Lower dissolved-oxygen concentrations in (figs. 8 and 9; table 2). Lithium concentration [(5 Hg/L) the summer samples may result from less turbulence in micrograms per liter] was higher in the Mill Creek the river than during winter stormflow, and may result sample. from the lower solubility of oxygen in warmer water. In addition to Stiff and Piper diagrams, the Also in summer, dissolved oxygen can be depleted by major-ion composition of water samples was evaluated biochemical processes, such as respiration by algae using boxplots. The variability of selected constituents that consume dissolved, suspended, or precipitated as well as differences between surface and ground organic matter. water can be observed from these boxplots (fig. 11). Boxplots show the range of values for a selected water- quality constituent. The vertical size of the box is deter- Ground Water mined by the range of the data, as in a histogram. The width of the box is meaningless and is for display pur­ Ground-water samples were collected from 25 poses only. The median and selected percentiles of the wells mostly on the Yucaipa plain (fig. 3) and from 1 data are indicated along with any outliers. well in San Timoteo Canyon. On the basis of these Phosphate showed the highest variability (rang­ samples, most ground water in the Yucaipa area shows ing from the upper 75 to the lower 25 percentile fig. 11) little areal variability and is of good quality by U.S. of any constituent sampled, perhaps as a result of the Environmental Protection Agency (EPA) drinking higher phosphate concentrations found in storm runoff water standards (U.S. Environmental Protection in Yucaipa Creek (table 2). Nitrate (NO3) Agency, 1994). Dissolved-solids concentrations ranged

22 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Dissolved Residue on oxygen pH evaporation 15 10 600 Outlier value of 712 not shown 10 9 400 mg/L mg/L 5 8 200 ANDARD UNITS ST

0 7 0 SW GW SW GW SW GW Sodium Potassium Magnesium Calcium 120 6 30 100 Outlier value of 200 not shown 80 4 20

50 mg/L as K mg/L as Na mg/L as Ca 40 2 mg/L as Mg 10

0 0 0 0 SW GW SW GW SW GW SW GW Chloride Fluoride Sulfate 40 2.0 100 Outlier value of 260 not shown 4

20 1.0 50 mg/L as F mg/L as Cl mg/L as SO

0 0 0 SW GW SW GW SW GW Barium Boron Iron Manganese 60 100 150 70 Outlier value Outlier value of 330 not of 2,300 not shown shown 50 40 100

50 30 H g/L as B H g/L as Fe mg/L as Ba 20 50 mg/L as Mn

10 0 0 0 0 SW GW SW GW SW GW SW GW Nitrite + Nitrate Phosphate 20 0.3 EXPLANATION Upper detached SW Surface-water samples Upper outside GW Ground-water samples 0.2 Upper 90 percent mg/L Milligrams per liter Upper 75 percent g/L Micrograms per liter 10 H Median mg/L as P mg/L as N 0.1 Lower 25 percent Lower 10 percent Lower outside 0 0 Lower detached SW GW SW GW

Figure 11. Concentration of selected constituents for selected wells and surface-water sites in the Yucaipa area, southern California.

Water Quality 23 Figure 12. Concentration of dissolved solids, nitrites plus nitrates, and dissolved oxygen for selected wells and surface-water sites in the Yucaipa area, southern California.

24 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Figure 12—Continued.

Water Quality 25 from 186 to 563 mg/L (table 3, at back of report; fig. that occur in the ponds before water infiltrates into the 12), with an outlier of 712 mg/L at well ground. 2S/2W-1J1. Sodium concentrations ranged from 14 to Three wells (1S/2W-34N1, 2S/2W-3E1, and 58 mg/L, with outliers of 120 mg/L and 200 mg/L at 2S/2W-4R1) located in the western part of the Yucaipa wells 2S/2W-28C2 and 2S/2W-1J1, respectively. Chlo­ area and one well (1S/1W-19G1) in the northern part of ride concentrations ranged from 6.3 to 36 mg/L, with the Yucaipa area yielded water with a high concentra­ an outlier of 65 mg/L at well 2S/2W-28C2. Sulfate con­ tion of nitrate (fig. 12). Water from three of these wells centrations ranged from 13 to 86 mg/L, with an outlier (19G1, 34N1, and 3E1) had nitrate concentrations that of 260 mg/L at well 2S/2W-1J1. Iron concentrations exceed the MCL of 10 mg/L as N; water from well ranged from less than the detection limit of 3 mg/L to 2S/2W-4R1 had a nitrate concentration of 9.6 mg/L, 140 mg/L, with an outlier of 2,300 mg/L, also at well just below the MCL. Water from these four wells also 2S/2W-1J1. This unusually high concentration of iron was higher in dissolved solids, sodium, calcium, chlo­ may result from corrosion of the steel well casing. The ride, sulfate, and bicarbonate. These wells are located sample from well 2S/2W-1J1 also showed signs of a downgradient from an area that has been used for agri­ reducing environment and had no dissolved oxygen, a culture (fig. 7). The high concentrations of these con­ condition that causes iron to become soluble. Boron stituents at well 1S/2W-34N1 may result from concentrations ranged from 20 to 70 Hg/L, with an out­ agricultural practices and evaporative processes. The lier of 330 Hg/L at well 2S/2W-1J1. lower concentrations of nitrate in wells 2S/2W-3E1 and As in surface water, calcium and bicarbonate 2S/2W-4R1 may result either from a different source of were the major ions found in ground water on the basis nitrate or from dilution with less contaminated water as ground water moves through the area. The later seems of milliequivalence (figs. 8 and 9B). Four wells were more plausible, suggesting a separate but converging not dominated by calcium and bicarbonate. Water from ground-water-flow path, possibly coincident with Oak well 2S/2W-1J1 was high in sodium, sulfate, and Glen Creek. dissolved-solids concentration and contained almost no magnesium. Water from this well also had elevated Most constituents analyzed in ground-water samples were below their respective MCL’s. All sulfate concentrations of fluoride and boron, which may indi­ concentrations, except for well 2S/2W-1J1, were below cate a contribution of mineralized ground water ema­ the Secondary Maximum Contaminant Level (SMCL) nating from a nearby fault zone. This explanation of 250 mg/L, as defined by the U.S. Environmental seems plausible because well 2S/2W-1J1 is located Protection Agency (1994). Water from one well near the intersection of the South Mesa and Casablanca (2S/2W-1J1) exceeded the SMCL for iron, which is Barriers (figs. 3 and 8). Wells 2S/2W-14R3 and 300 Hg/L. Water from two wells (1S/1W-19G1 and 2S/2W-24L1 yielded water having more than 2S/2W-28C2) exceeded the SMCL for manganese, 80 percent sodium and potassium and less than which is 50 Hg/L. Barium concentration in all water 20 percent calcium and magnesium (fig. 9B). These samples was far below the MCL of 2,000 Hg/L. two wells are located south of the Banning and Cherry In general, sodium, calcium, magnesium, chlo­ Valley Faults (figs. 3 and 8). Ground water moving to ride, nitrate, sulfate, and dissolved-solids concentra­ these wells probably has a geochemical signature more tions were higher in ground water than in surface water representative of the unconsolidated nonmarine sedi­ (fig. 11) probably as a result of dissolution of minerals ment of the badlands than of the crystalline rocks found in the aquifer matrix. However, concentrations of iron, in the other hills and mountains in the Yucaipa area. manganese, and phosphate were higher in surface Well 2S/2W-28C2 is located in San Timoteo Canyon, water than in ground water. which is eroded into the badlands, and has the same water type as well 2S/2W-24L1 (fig. 9B). Well Flowmeter Data 2S/2W-28C2 is located near and probably downgradi­ ent from fishing ponds. The elevated concentrations of Flowmeter data were collected from well sodium, calcium, chloride, and bicarbonate in water 1S/2W-25R4 using a commercial, vertical-axis current from this well may result from evaporative processes meter, commonly called a spinner tool. This tool

26 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 measures the velocity of water flowing inside the well entered the well at a nearly uniform rate between casing by recording the number of revolutions per depths of 600 and 820 ft. Virtually no water entered the second made by a spinning impeller. Flowmeter data well between depths of 820 and 950 ft. Because the are helpful in determining the water-yielding character- water table was at a depth of about 300 ft below land istics of aquifer material opposite the screened interval surface, it is likely that some additional contribution of and in evaluating mixtures of water collected at differ- water to the well would have occurred if the well were ent depths within the well. A continuous profile of perforated above a depth of 450 ft. velocity was recorded for the entire depth of the well, Variations in water yield can be caused by many and static data (stop counts) were collected every 10 ft. factors such as the hydraulic characteristics of adjacent Flowmeter data for well 1S/2W-25R4 demon- aquifer material or any encrustation of the well screen. strate that water does not enter the well in a uniform The inferred change in aquifer characteristics at about manner (fig. 13). Rather, the data suggest that there are 600 ft is not evident from the driller’s or electric logs, three distinct zones. About one-half of the total dis- but the change at 820 ft is supported by a change in sig- charge from the well entered the casing through the top nature of the 16-inch normal resistivity log (fig. 13). 150 ft of perforations—that is, between depths of 450 The material below 820 ft appears to have thinner lay- and 600 ft below land surface. The rest of the discharge ering and a higher percentage of clay. These observed

16-inch Driller's Spontaneous normal Vertical Well Water- Tritium log potential resistivity flow rate construction quality (picocuries (millivolts) (ohm-meters) (percent) sampling per liter) depth -350 -150 0 250 0 100 0 B 2.1

100

ACE 200

300

400

500 3.9� � 600 <0.3� � 700 � 0.4� 800 0.8�

DEPTH, IN FEET BELOW LAND SURF � 900 1.4

1,000

EXPLANATION Driller's log Well construction Water level� Water-quality� � sampling depth Clay Blank casing Static Pump intake Pumping B Bulk sample Silt and sand Perforated� Point sample casing Pumping rate -� Direction of� 750 gallons per� Gravel flow in well minute

Figure 13. Driller’s log, electric logs, vertical flow rate, well construction, and water-quality sampling for well 1S/2W-25R4 in the Yucaipa area, southern California.

Water Quality 27 changes in flow rate and possible changes in lithology Results of the depth-dependent sampling show were used to select specific depths at which to sample that the general water chemistry for the samples from water quality. well 1S/2W-25R4 are almost identical. Stiff diagrams of each sample collected at the different depths are sim­ Depth-Dependent Samples ilar to the Stiff diagram of the bulk sample shown in figure 8. This small vertical variability in general water Depth-dependent and bulk samples for chemical chemistry can be explained in at least two ways. First, and isotopic analyses were collected from production the geologic materials adjacent to the perforated inter­ wells (table 3). Production wells generally have long vals may be chemically similar despite their hydraulic screened intervals and can be open to more than one differences (fig. 13). Second, ground water flowing in geologic or hydrogeologic unit. Bulk samples from this recharge area near the mountains may not have had production wells typically are a mixture of ground sufficient time to convert into chemically different, ver­ water from different units; nevertheless, only bulk sam­ tically stratified compositions. ples were obtained for production wells sampled in this Some vertical differences, however, were noted. study, except for well 1S/2W-25R4, because of the The dissolved-oxygen concentrations were highest expense and difficult logistics of depth-dependent sam­ near the water table and lowest at the bottom of the pling. well. The concentration of nitrate and nitrite also At well 1S/2W-25R4, depth-dependent chemical decreased with depth. Dissolved-solids and chloride and flowmeter data were collected using special sam­ concentrations tended to peak in the middle depths of ple-collection techniques while the well was pumped. the well. These results suggest that the most active part All depth-dependent water samples and one bulk sam­ of the ground-water flow system is near the top of the ple were collected while the production well was dis­ well. charging at a rate of 750 gal/min. To facilitate this Tritium, a naturally occurring radioactive iso­ discrete-depth sampling, the well had been modified tope of hydrogen, was used to determine the age (time with a temporary, lower capacity pump. A second bulk since recharge) of the ground water. Tritium activity sample was collected while the well was pumped at a above the detection level of 0.3 pCi/L (picocuries per liter) was used as an indication of ground water rate of 1,450 gal/min using the standard-capacity pro­ recharged since 1952. Some processes that could affect duction pump. Depth-dependent water samples were tritium values are dispersion, mixing with different collected using a high-pressure hose equipped with a waters, and degassing during sampling. All depth- one-way valve that allows water to enter from a specific dependent samples from well 1S/2W-25R4 were ana­ depth (Gossell and others, 1995; Izbicki and others, lyzed for tritium. The highest tritium value (3.9 pCi/L) 1999). The hose is lowered to the desired depth, the came from the shallowest sample depth, indicating that valve is opened, and the sample is collected. Then the at least some of this water was recharged since 1952 hose is retrieved from the well, and the sample water is (fig. 13). The other samples ranged from less than the collected from the hose at land surface. Prior to sample detection limit of 0.3 pCi/L at 590 ft to 1.4 pCi/L collection, the well was pumped for over 12 hours to (fig. 13 and table 3) at the bottom of the well. ensure that ground water entering the well through the The presence of an elevated value of tritium at screened interval was representative of the aquifer. the bottom of the well is unlikely, because it implies All samples were collected below the pump that younger water is present at the top and bottom of intake. The sample collected from the deepest part of the well. A more likely explanation is that the bottom the screened interval is interpreted as representing of the well is inactive and was not purged of water dur­ water entering below that depth. Water sampled above ing pumping. This explanation is consistent with the the lowest sample depth and below the pump intake is flowmeter data showing that virtually no water enters a mixture of water in the well at the first sample depth the well below a depth of about 820 ft. If this explana­ and water that entered the well between the two sample tion is correct, then all water-chemistry data collected depths. The proportions of water in that mixture can be for depths at 820 and 900 ft represent largely unpurged determined from the flowmeter data. water originating from shallower perforated intervals.

28 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Tritium values for the bulk samples were 2.1 pCi/L for ISOTOPIC COMPOSITION OF WATER a pumping rate of 750 gal/min and 3.4 pCi/L for a pumping rate of 1,450 gal/min. The higher tritium value for the higher pumping rate indicates that more Oxygen-18 and Deuterium water is being withdrawn from the uppermost zone. Surface-water isotopes at a particular site have a Depth-dependent samples at the lower pumping wide range of values (fig. 14A) which are highly influ­ rate (750 gal/min) also were analyzed for 14C (table 3). enced by the direction from which storms are generated The collected water samples are relatively young given and over time will approximate the values of ground the time scale for waters dated using 14C. Expressed as water. Although all three storms originated in the north- percent modern carbon, the 14C value was 86.1 in the west, the first and second storms entered the basin from the west and moved northeastward (fig. 10). The third well where no tritium (< 0.3 pCi/L) was detected (fig. 14 storm entered the basin from the north and produced 13). Assuming radioactive decay, with an initial C much more precipitation than did the first two storms. activity of 90 percent modern carbon (Izbicki and oth­ The third storm had warm moist air drawn into the sys­ ers, 1997, p. 16) and neglecting reactions with the aqui­ tem from the west. This effect typically occurs later in fer material, this sample has an approximate time of the rainy season and produces many of the larger mag­ recharge of less than 400 years before present. nitude, longer duration storms. Because the moist air A simple three-cell mixing model can be used to from the storm is generated from a lower latitude and warmer climate than is air from the north, the precipi­ test the data and interpretations of the depth-dependent tation is isotopically heavier (fig. 14). sampling. If Q , Q , and Q are the discharge rates for 1 2 3 Isotopic values for base flow (table 2) plot the upper, middle, and lower zones, respectively; and slightly above the meteoric water line (fig. 14B), and C1, C2, and C3 are concentrations of a selected constit­ mean isotope ratios are −10.3 and −69.0 for δ18O and uent for the same zones, then δD, respectively. The mean isotopic ratios for the first storm are −12.7 and −91.8 for δ18O and δD, respec­ Q C = Q C + Q C + Q C , (1) tively. These values are grouped below the meteoric T T 1 1 2 2 3 3 water line near the bottom of the graph and indicate that this runoff is isotopically much lighter than is base where QT and CT are total discharge and concentration flow. The mean isotope ratios for the second storm are from the well. Using flowmeter and tritium −11.7 and −77.3 for δ18O and δD, respectively, and are data, grouped above the meteoric water line and slightly below the middle of the graph. The mean isotopic ratios 18 750 (2.1) = 375 (3.9) + 375 (0) + 0 (1.4), or (2A) for the third storm are −6.51 and −38.2 for δ O and δD, respectively, and are grouped above the meteoric water line, near the top of the graph. Runoff from this 375%3.9& storm is isotopically much heavier than is base flow. 2.1 ∼ ------, (2B) 750 Over time, the isotopic ratio of water vapor in different storms trends to an average value; therefore, which suggests that the assumed contribution from the isotopic ratio of ground water is determined prima­ each zone to total discharge is reasonable. Applying the rily by local differences in the temperature of conden­ sation of water vapor, prior to its being recharged in same test to other constituents (alkalinity, sulfate, different places and at different times. The deuterium nitrate) yielded similar results. Additional depth- content of precipitation varies seasonally as well as by dependent samples from nearby wells might help ver­ storm and is highly dependent on storm- track trajecto­ ify these results and extend analysis to other parts of the ries (Friedman and others, 1992). The δ18O and δD Yucaipa area. ratios of water from most wells ranged from −8.11

Isotopic Composition of Water 29 A -20 Isotopic composition by site -30

-40 Evaporative trend line -50 28C2 (San Timoteo Canyon) -60 Local ground-water line δ D), IN PER MIL Ground-water sites -70 Oak Glen Creek A� Upper Ford Canyon B� in Ford Canyon -80 C� near Oak Glen at 2nd Street

A DEUTERIUM ( D T Meteoric water line -90 Yucaipa Creek

DEL (Craig, 1961) E� at Mesa Grande F� at 5th Street -100 G below Dunlap Acres H Mill Creek outlet at Regional Park -110 -14 -13 -12 -11 -10 -9 -8 -7 -6 -5 -4 DELTA OXYGEN-18 (δ 18O), IN PER MIL B -20 Isotopic composition by storm -30 Third storm -40 Evaporative trend line 28C2 -50 (San Timoteo Canyon)

-60 Local ground-water line δ D), IN PER MIL

-70 Second storm Ground-water sites -80 Base flow A DEUTERIUM (

T Meteoric water line -90 (Craig, 1961) Stormflow DEL February 3, 1998 February 19, 1998 First storm -100 February 23, 1998

-110 -14 -13 -12 -11 -10 -9 -8 -7 -6 -5 -4 DELTA OXYGEN-18 (δ 18O), IN PER MIL

18 Figure 14. Isotopic concentrations of delta deuterium (∂D) compared to delta oxygen-18 (∂ O) by site (A) and by storm (B) for selected wells and surface-water sites in the Yucaipa area, southern California.

30 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 to −9.97 per mil and from −53.8 to −65.5 per mil, the highest value found in ground-water samples. Well respectively, and the values are tightly grouped above 2S/2W-3E1 is located along Oak Glen Creek, which the meteoric water line. The average δ18O and δD may be a source of recharge to the well. ratios of surface water samples was −10.2 and −68.3 In water from wells 2S/2W-4G3, 2S/2W-4G4, per mil which approximate ground-water values. The and 2S/2W-4J2, tritium activity was less than the detec­ isotopic ratio of water from wells plots along a local tion limit of 0.3 pCi/L. These wells are located at the ground-water line about 1 per mil above, and parallel west end of Yucaipa in the Western Heights subbasin to, the meteoric water line. Similar data from and have the oldest water sampled. The depth of two of Woolfenden (1994) and Izbicki and others (1997) cor­ the three wells is greater than 1,000 ft (1,690 and roborate the local ground-water line for the western 1,090 ft), and the wells may be extracting a greater pro- slope of the San Bernardino Mountains. Snow and, in portion of deeper, older ground water than other, shal­ turn, snowmelt have been shown to plot above the lower wells. The Western Heights subbasin, in meteoric water line (Magaritz and others, 1989). The particular Dunlap Acres, also historically had a pump­ heaviest (least negative) water sampled, with respect to 18 ing depression, which is caused by ground-water δ O, is from well 2S/2W-28C2. Because the well is extractions exceeding recharge. The pumping depres­ near fishing ponds, water moving to the well may have sion, the absence of tritium, and the greater distance of been partly evaporated prior to being recharged. An this area from the greater precipitation found in the San evaporative trend line can be drawn from well Bernardino Mountains suggests that Dunlap Acres 2S/2W-28C2 to a point that intersects the local ground- receives less recharge than other parts of the Yucaipa water line near the mean value (fig. 14). area.

Tritium LIMITATIONS AND FUTURE NEEDS Tritium activity in water from wells (table 3 and fig. 15) in the Yucaipa area ranged from less than the The primary limitation of this study is the small detection limit of 0.3 to 15 pCi/L, and tritium activity number of vertically discrete ground-water samples in water from surface-water sites (table 2) ranged from that were obtained. No multiple-depth monitoring 7.3 to 18 pCi/L. Tritium activity in 27 of 31 well sam­ wells were available in the Yucaipa area at the time of ples ranged from 0.7 to 15 pCi/L, indicating that all or this study. Since sampling was done for this study, part of the pumped water was recharged after 1952. some multiple-depth monitoring wells have been Many of these wells are located on the Yucaipa plain installed. If these wells were sampled for the same and likely extract ground water from a water-bearing chemical constituents, the data likely would aid in zone that is hydraulically connected to areas of recent understanding the vertical and horizontal characteris­ recharge (fig. 15). Tritium activity in water from wells tics of ground-water flow in the Yucaipa area. Depth- near the hills and mountains—in particular north of the dependent sampling of production wells is logistically Oak Glen Fault, or east of the Casa Blanca Fault and challenging, but can yield excellent flow and water- north of the South Mesa Barrier— ranged from 7.2 to quality data to compare with water-level and water- 11 pCi/L. These values are similar to surface-water quality data from multiple-depth monitoring wells. samples, and probably indicate that most pumped The second major limitation of this study is the water was recharged recently. lack of detailed, ground-water-level maps—ideally for Tritium activity in water from well 2S/2W-28C2 different time periods and for each significant hydro- was 7.8 pCi/L. The proximity of the well to the fishing geologic unit in the Yucaipa area. Because areal and ponds, as well as the general chemistry data and the vertical ground-water-level data are sparse, and the anomalous δ18O and δD data, suggests that the ponds arrangement of subbasins is complex, this mapping may be a source of recharge to the well. The tritium may need to be done iteratively with development of a activity in water from well 2S/2W-3E1 was 15 pCi/L, ground-water flow model.

Limitations and Future Needs 31 18 Figure 15. Delta deuterium (δD), delta oxygen-18 (δ O), and tritium activity in selected wells and surface-water sites in the Yucaipa area, southern California.

32 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Figure 15—Continued.

Limitations and Future Needs 33 SUMMARY AND CONCLUSIONS area—Geology, hydrology, and operation–economics studies: California Department of Water Resources Most water sampled in the Yucaipa area is a Bulletin 104-5, 75 p. calcium-bicarbonate type. The general chemical com­ ———1979, Preliminary evaluation of State Water Project position of surface water resembles that of ground ground-water storage program, Bunker Hill–San water, although the concentrations of most constituents Timoteo–Yucaipa basins: 82 p. are higher in ground water. The ionic strength of most ———1986, San Bernardino–San Gorgonio water resources ground-water samples was similar. Elevated concentra­ management investigation: Southern District, 83 p. tions of nitrate were found in some ground-water sam­ Camp, Dresser, and McKee, 1994, Water facilities master ples from wells and may indicate recharge of water plan for the Yucaipa Valley Water District: Final water master plan report [variously paged]. from agricultural areas. Water samples from nearby Craig, H., 1961, Isotope variation in meteoric waters: Sci­ wells suggest that the elevated nitrate concentrations ence, v. 133, p. 1702–1703. are diluted by ground water that originates as recharge Dutcher, D.L., and Burnham, W.L., 1959, Geology and from Oak Glen Creek. ground-water hydrology of the Mill Creek area, San Ground water was found to have a range of tri­ Bernardino County, California: U.S. Geological Survey tium activity, indicating different times since recharge Open-File Report, 229 p. and possible mixing along ground-water flow paths. Dutcher, D.L., and Fenzel, F.W., 1972, Ground-water out- The oldest water had tritium values less than 0.3 pCi/L, flow, San Timoteo–Smiley Heights area, Upper Santa indicating more than 50 years since recharge. Tritium Ana Valley, southern California, 1927 through 1968: values greater than 0.3 pCi/L indicate that at least part U.S. Geological Survey Open-File Report 72-0097, of the pumped water was recharged since 1952. Ground 30 p. water near the hills and mountains—in particular, Eckis, Rollin, 1934, Geology and ground-water storage ground water that is north of the Oak Glen Fault, or east capacity of valley fill, South Coastal Basin Investiga­ tion: California Division of Water Resources Bulletin of the Casa Blanca Barrier and north of the South Mesa 45, 273 p. Barrier—had tritium values similar to those of surface- Egan and Associates, Inc., 1989, Plan of water system devel­ water samples and indicates that it is likely to be the opment: Report to Western Heights Water Company most recently recharged ground water. [variously paged]. Flowmeter data from well 1S/2W-25R4 showed Fishman, M.J., 1993, Methods for analysis by the United that more than one-half of the water flowed into the States Geological Survey National Water Quality Labo­ well between depths of 450 and 600 ft below land sur­ ratory—Determination of inorganic and organic con­ face. At a flow rate of 750 gal/min, virtually no water stituents in water and fluvial sediments: U.S. was contributed to the well below a depth of about 820 Geological Survey Open-File Report 93-125, 217 p. ft. Water recharged since 1952 was found in the upper- Fishman, M.J., and Friedman, L.C., eds., 1989, Methods for most part of the well. Water flowing into the well from determination of inorganic substances in water and flu­ depths below 590 ft probably was recharged more than val sediments: Techniques of Water-Resources Investi­ gations of the United States Geological Survey, book 5, 50 years and less than about 400 years before present. chap. A1, 545 p. Tritium and flowmeter data from well 1S/2W-25R4 Fletcher, G.L., 1976, Fluctuation of water levels in wells in suggest that the well could extract additional water if the Yucaipa area, 1965–75: San Bernardino Valley perforations were present between the water table at a Municipal Water District, Report No. ENG–76–E2, depth of about 300 ft below land surface and the top of 17 p. existing perforations at a depth of 450 ft. Fox, R.C., 1987, A hydrogeologic analysis and projected water level decline in Western Heights subbasin: A report for Western Heights Water Company, 21 p. SELECTED REFERENCES ———1990, Groundwater resources monitoring plan: A report for Yucaipa Valley Water District, v. 1, 136 p. Burnham, W.L., and Dutcher, L.C., 1960, Geology and Friedman, I., Smith, G.I., Gleason, J.D., Warden, A., and ground-water hydrology of the Redlands–Beaumont Harris, J.M., 1992, Stable isotope composition of area, California, with special reference to ground-water waters in southeastern California: Journal of Geophys­ outflow: U.S. Geological Survey Open-File Report, ical Research, v. 97, no. D5, p. 5795–5812. 352 p. Gonfiantini, R., 1978, Standards for stable isotope measure­ California Department of Water Resources, 1970, Meeting ments in natural compounds: Nature, v. 271, water demands in the Bunker Hill–San Timoteo p. 534–536.

34 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Gossell, M.A., Hanson, R.T., Izbicki, J.A., and Nishikawa, Michel, R.L., 1976, Tritium inventories of the world’s Tracy, 1995, Application of impeller-flow meter and oceans and their implications: Nature, v. 263, p. discrete water-sampling techniques for improved 103–106. ground-water well construction [abs.]: Eos, v. 76, ———1989, Tritium deposition in the continental United no. 46, p. 182. States, 1953–1983: U.S. Geological Survey Water- Harden, D.R., 1998, California Geology: Upper Saddle Resources Investigations Report 89-4072, 46 p. River: New Jersey, Prentice-Hall, Inc., 479 p. Moreland, J.A., 1970, Artificial recharge, Yucaipa, Califor­ Horowitz, A.J., Demas, C.R., Fitzgerald, K.K., Miller, T.L., nia: U.S. Geological Survey Open-File Report, 44 p. and Rickert, D.A., 1994, U.S. Geological Survey proto­ Morton, D.M., 1974, Generalized geologic map of south- col for the collection and processing of surface-water western San Bernardino County, California, plate 1B, in samples for the subsequent determination of inorganic Fife, D.L., Rodgers, D.A., Chase, G.W., Chapman, constituents in filtered water: U.S. Geological Survey R.H., and Sprotte, E.C., 1976, Geologic hazards in Open-File Report 94-539, 57 p. southwestern San Bernardino County, California: Cali­ fornia Division of Mines and Geology Special Report International Atomic Energy Agency, 1981, Stable isotope 113, 40 p. hydrology: Deuterium and oxygen-18 in the water Patton, C.J., and Truitt, E.P., 1992, Methods of analysis by cycle: Technical Reports Series No. 210, 337 p. 18 the United States Geological Survey National Water Izbicki, J.A., 1996, Use of O and D to define seawater Quality Laboratory—Determination of total phospho­ intrusion, in Bathala, C.T., ed., North America Water rus by a Kjeldahl digestion method and an automated and Environment Congress, Anaheim, California, June colorimetric finish that includes dialysis: U.S. Geologi­ 23–28, Proceedings: New York, American Society of cal Survey Open-File Report 92-146, 39 p. Civil Engineers, 1 CD-ROM. Piper, A.M., 1944, A graphic procedure in the geochemical Izbicki, J.A., Christensen, A.H, and Hanson, R.T., 1999, U.S. interpretation of water analyses: American Geophysical Geological Survey combined well-bore flow and depth- Union Transactions, v. 25, p. 914–923. dependent water sampler, U.S. Geological Survey Fact Powers, W.R., III, and Hardt, W.F., 1974, Oak Glen water Sheet 196-99, 2 p. resources development study using modeling tech­ Izbicki, J.A., Danskin, W.R, and Mendez, G.O., 1997, niques, San Bernardino County, California: U.S. Geo­ Chemistry and isotopic composition of ground water logical Survey Water-Resources Investigations Report along a section near the Newmark area, San Bernardino 31-74, 59 p. County, California, U.S. Geological Survey Water- Stiff, H.A., Jr., 1951, The interpretation of chemical water Resources Investigations Report 97-4179, 27 p. analysis by means of patterns: Journal of Petroleum Magaritz, M., Aravena, R, Pena, H., Suzuki, O., and Grilli, Technology, v. 3, no. 10, p. 15–17. A., 1989, Water chemistry and isotopic study of streams Struzeski, T.M., DeGiacomo, W.J., and Zayhowski, E.J., and springs in northern Chile: Journal of Hydrology, 1996, Methods of analysis by the United States Geolog­ v. 108, p. 323–341. ical Survey National Water Quality Laboratory—Deter­ Mann, J.F., Jr., 1986, Revised safe yield of the Yucaipa sub- mination of dissolved aluminum and boron in water by basins: San Bernardino Valley Muncipal Water District, inductive coupled plasma-atomic emission spectrome­ unpub. report, 7 p. try: U.S. Geological Survey Open-File Report 96-149, 17 p. Mann, J.F., Jr., and Todd, D.K., 1990, Perennial yield, Todd, D.K., 1988, Perennial yield of the Yucaipa groundwa­ Yucaipa groundwater basin: San Bernardino Valley ter basin: Report to Yucaipa Valley Water District, 71 p. Muncipal Water District and Yucaipa Valley Water Dis­ U.S. Environmental Protection Agency, 1994, Drinking trict, unpub. report, 4 p. water standards and health advisories table: U.S. Envi­ Matti, J.C., and Carson, S.E., 1991, Liquefaction susceptibil­ ronmental Protection Agency, Region IX, San Fran­ ity in the San Bernardino Valley and vicinity, southern cisco, California, 25 p. California—A regional evaluation: U.S. Geological Wilde, F.D.,and Radtke, D.B., eds., 1998, National field Survey Bulletin 1898, 53 p. manual for the collection of water-quality data: U.S. Matti, J. C., Morton, D.M., Cox, B.F., Carson, S.E., and Geological Survey Techniques of Water-Resources Yetter, T.J., 1992, Geologic map of the Yucaipa quad­ Investigations, book 9, chap. A6, 218 p. rangle, San Bernardino and Riverside Counties, Cali­ Woolfenden, L.R., 1994, Oxygen-18, deuterium, and tritium fornia: U.S. Geological Survey Open-File Report 92- as tracers of imported water in the Rialto–Colton Basin, 446, 14 p. and 1 map sheet. California, in Marston, R.A. and Hasfuther, V.R., Mendenhall, W.C., 1905, The hydrology of San Bernardino Effects of human-induced changes on hydrologic sys­ Valley, California: U.S. Geological Survey Water- tems: American Water Resources Association, Supply Paper 142, 124 p. p. 923–932.

Selected References 35 Table 2. Chemical and isotopic analyses of water from selected surface-water sites in the Yucaipa area, southern California [USGS, U.S. Geological Survey; ft3/s, cubic foot per second; HS/cm, microsiemen per centimeter at 25 °C; mg/L, milligram per liter; °C, degree Celsius; B, base flow; Hg/L, micrograms per liter; pCi/L, picocurie per liter; per mil, parts per thousand; <, less than; —, no data] Specific Discharge pH, field USGS station name USGS station number Date Time conductance (ft3/s) (standard units) (HS/cm) Upper Oak Glen Creek in Ford Canyon 340326116560501 4/30/98 1715 0.31B 216 7.8 Oak Glen Creek in Ford Canyon 340326116560601 7/31/97 0940 .60B 351 8.4 Oak Glen Creek near Oak Glen 340307116592101 2/3/98 1645 2.2 260 8.3 1/13/98 0750 .79B 395 8.5 1/3/97 1040 1.4 361 8.5 Oak Glen Creek at 2nd St. 340238117023201 2/23/98 1545 6.9 190 8.5 2/23/98 1330 2.3 384 8.6 2/3/98 1615 4.3 117 7.9 Yucaipa Creek at Mesa Grande Bridge 340051117002601 2/23/98 2115 100 74 7.5 2/19/98 2245 15 63 7.6 Yucaipa Creek at 5th St. 340049117031401 2/23/98 2200 110 75 7.8 2/20/98 0010 26 55 7.9 2/3/98 1530 2.4 78 7.7 Yucaipa Creek below Dunlap Acres 340037117064301 2/3/98 1430 190 172 8.3 Mill Creek at Yucaipa Regional Park 340316117025101 7/10/96 1330 1.0B 240 8.1

Oxygen, Temp- Temp- Calcium, Magnesium, Sodium, dissolved erature, erature, dissolved dissolved dissolved (mg/L) air (°C) water (°C) (mg/L) (mg/L) (mg/L) Upper Oak Glen Creek in Ford Canyon — 15.5 7.5 24 9.4 4.4 Oak Glen Creek in Ford Canyon 8.5 17.0 12.5 40 15 7.6 Oak Glen Creek near Oak Glen — 5.5 6.5 30 9.6 8.1 10.8 6.0 7.5 45 16 15 — 13.0 12.0 43 14 12 Oak Glen Creek at 2nd St. — 11.0 11.0 23 7.6 6.7 9.4 13.0 12.5 — — — — 6.0 7.0 13 3.8 3.8 Yucaipa Creek at Mesa Grande Bridge — 10.0 9.0 8.3 2.1 2.4 — 9.0 7.0 6.9 1.8 2.2 Yucaipa Creek at 5th St. — 11.0 7.0 8.9 2.3 3.1 — 7.0 6.5 5.8 1.5 2.2 — 10.0 8.5 9.1 2.2 2.8 Yucaipa Creek below Dunlap Acres 10.6 12.0 11.0 20 4.3 5.2 Mill Creek at Yucaipa Regional Park 8.2 32.5 15.5 28 5.7 4.7

36 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Table 2. Chemical and isotopic analyses of water from selected surface-water sites in the Yucaipa area, southern California—Continued

Potassium Alkalinity, Sulfate, Chloride, Fluoride, Bromide, USGS station name dissolved field dissolved dissolved dissolved dissolved (mg/L) (mg/L as CaCO3) (mg/L) (mg/L) (mg/L) (mg/L) Upper Oak Glen Creek in Ford Canyon 2 98 6.7 1.6 0.7 <0.01 Oak Glen Creek in Ford Canyon 3 160 17 2.2 .8 <.01 Oak Glen Creek near Oak Glen 2 99 22 4.3 .8 <.01 2 150 32 7.7 .5 .02 2 130 37 6.2 .5 — Oak Glen Creek at 2nd St. 2 — 17 3.3 .3 <.01 — — — — — — 2 45 7.8 2.5 .2 <.01 Yucaipa Creek at Mesa Grande Bridge .9 27 2.2 1.7 .1 <.01 .9 24 1.9 1.6 .1 <.01 Yucaipa Creek at 5th St. .9 34 2.5 1.7 .1 <.01 .7 22 1.4 1.3 .1 <.01 1 28 3.2 1.4 .2 <.01 Yucaipa Creek below Dunlap Acres 1 43 22 2.5 .3 <.01 Mill Creek at Yucaipa Regional Park 2 84 13 1.2 .8 <.01

Iodide, Silica, Residue at Nitrite, NO2 + NO3, Ammonia, dissolved dissolved 180°C dissolved dissolved dissolved (mg/L) (mg/L) (mg/L) (mg/L as N) (mg/L as N) (mg/L as N) Upper Oak Glen Creek in Ford Canyon <0.001 7.0 120 0.01 0.19 0.05 Oak Glen Creek in Ford Canyon <.001 10 200 <.01 .21 <.01 Oak Glen Creek near Oak Glen .001 11 162 <.01 .92 <.02 .001 21 249 <.01 2.3 .03 .001 17 227 .03 1.5 .08 Oak Glen Creek at 2nd St. .002 8.5 124 <.01 1.5 .07 — — — — — .001 4.3 74 <.01 .41 .04 Yucaipa Creek at Mesa Grande Bridge .001 4.4 51 <.01 .67 .06 .001 3.3 41 <.01 .53 <.02 Yucaipa Creek at 5th St. .001 5.2 55 <.01 .97 <.02 .001 3.2 40 <.01 .57 .04 .002 3.2 57 .01 1.6 .09 Yucaipa Creek below Dunlap Acres .002 3.3 108 .03 1.8 .09 Mill Creek at Yucaipa Regional Park <.001 12 137 <.01 .18 .02

Table 2 37 Table 2. Chemical and isotopic analyses of water from selected surface-water sites in the Yucaipa area, southern California—Continued Phosphorus Ammonia + Phosphorus, Arsenic, Barium, Boron, Iron, ortho, USGS station name organic, dissolved dissolved dissolved dissolved dissolved dissolved (mg/L as N) (mg/L as P) (Hg/L) (Hg/L) (Hg/L) (Hg/L) (mg/L as P) Upper Oak Glen Creek in Ford Canyon <0.10 <0.01 0.02 <1 5.3 <16 <10 Oak Glen Creek in Ford Canyon <.20 <.01 <.01 <1 20 7 <3 Oak Glen Creek near Oak Glen .20 .03 .05 <1 12 22 21 .13 .04 .03 <1 18 <16 <10 <.20 .02 .02 <1 19 20 14 Oak Glen Creek at 2nd St. .30 .04 .05 <1 7.0 22 <10 — — — — — — — .37 .05 .05 <1 7.0 19 100 Yucaipa Creek at Mesa Grande Bridge .46 .21 .19 <1 7.0 20 34 .46 .20 .20 <1 6.0 <16 48 Yucaipa Creek at 5th St. .43 .21 .20 <1 5.7 18 25 .35 .22 .22 <1 4.3 19 110 .61 .23 .27 <1 6.0 23 52 Yucaipa Creek below Dunlap Acres .67 .19 .20 <1 8.0 24 29 Mill Creek at Yucaipa Regional Park <.20 <.01 .01 <1 10 9 <3

Lithium, Manganese, Strontium, H-2/H-1 O-18/O-16 Tritium, dissolved dissolved dissolved isotope ratio isotope ratio total (Hg/L) (Hg/L) (Hg/L) (per mil) (per mil) (pCi/L) Upper Oak Glen Creek in Ford Canyon <4 9 80 −63.3 −9.87 14 Oak Glen Creek in Ford Canyon <4 <1 190 −70.7 −10.48 7.3 Oak Glen Creek near Oak Glen <4 15 120 −92.4 −12.73 — <4 9 180 −63.5 −9.59 — <4 3 190 −59.7 −8.85 9.2 Oak Glen Creek at 2nd St. <4 8 110 −32.8 −5.58 — — — — — — — <4 5 60 −99.9 −13.61 — Yucaipa Creek at Mesa Grande Bridge <4 4 50 −38.9 −6.95 — <4 6 50 −77.9 −11.74 — Yucaipa Creek at 5th St. <4 <4 50 −42.8 −7.01 — <4 8 40 −76.6 −11.60 — <4 6 60 −99.0 −13.14 — Yucaipa Creek below Dunlap Acres <4 4 100 −75.8 −11.23 — Mill Creek at Yucaipa Regional Park 5 1 70 −78.6 −11.30 18

38 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Table 3. Chemical and isotopic analyses of water from selected wells in the Yucaipa area, southern California [State well number, see “Well-Numbering System” in text; USGS, U.S. Geological Survey; gal/min, gallons per minute; ft blw LSD, feet below land-surface datum; HS/cm, microsiemen per centimeter at 25 °C; mg/L, milligram per liter; Hg/L, microgram per liter; pCi/L, picocurie per liter; per mil, parts per thousand; °C, degree Celsius; B, bulk sample; <, less than; —, no data] Depth to Specific pH, field Oxygen, Flow rate Temperature, Temperature, State well number USGS station number Date Time sample conductance (standard dissolved (gal/min) air °C water °C (ft blw LSD) (HS/cm) units) (mg/L) 1S/1W-19G01 340415117012701 7/29/97 1330 180 — 745 7.3 6.9 25.0 18.5 1S/1W-27L01 340312116583901 7/29/97 0930 240 — 568 7.1 4.1 19.5 14.0 1S/1W-32C01 340253117002701 7/29/97 1145 90 — 476 7.2 6.0 23.0 16.5 1S/2W-24C02 340438117024201 7/31/97 1230 — — 650 7.4 6.5 32.5 20.0 1S/2W-25A01 340343117021201 7/17/97 1330 260 — 584 7.6 8.0 — 21.5 1S/2W-25R04(B) 340255117021601 2/25/98 1600 750 — 477 7.6 — 11.0 19.0 -25R04 340255117021601 2/25/98 1730 750 480 458 7.4 8.2 10.5 11.0 -25R04 340255117021601 2/25/98 1930 750 590 491 7.4 7.5 6.0 13.5 -25R04 340255117021601 2/25/98 2100 750 770 510 7.5 7.4 3.5 12.0 -25R04 340255117021601 2/25/98 2330 750 820 513 7.5 6.0 2.5 12.0 -25R04 340255117021601 2/26/98 0030 750 900 486 7.4 6.0 2.5 12.5 -25R04(B) 340255117021601 5/1/98 1000 1450 — 463 7.6 8.2 13.5 19.5 1S/2W-34N01 340202117050201 7/10/96 1430 600 — 831 7.6 5.6 32.0 20.5 1S/2W-36G01 340236117023101 7/18/97 0950 1,700 — 466 7.6 6.9 — 20.0 2S/1W-08F01 340054117002901 7/16/97 1210 250 — 601 7.2 5.8 — 18.0 2S/1W-15F02 340003116582501 7/16/97 1430 140 — 445 7.8 .4 — 20.0 2S/2W-01J011 340124117021301 6/2/98 1945 2.5 — 1,100 7.8 .0 24.5 22.5 2S/2W-02M01 340129117035101 7/15/97 1200 550 — 569 7.7 8.5 — 20.5 -02M01 340129117035101 7/10/98 1210 550 — 553 7.7 — 29.5 20.0 2S/2W-03E01 340148117045401 7/9/96 1330 1,200 — 734 7.5 6.0 30.0 20.0 2S/2W-03L01 340129117044201 7/11/96 1120 450 — 498 7.7 9.2 30.0 19.5 2S/2W-04G03 340144117053601 7/10/96 1020 1,000 — 477 7.6 4.8 29.0 19.0 2S/2W-04G04 340137117053501 4/30/98 1430 1,550 — 417 7.6 3.4 29.0 21.5 2S/2W-04J02 340135117051601 7/10/96 0900 2,000 — 455 7.7 5.2 30.0 19.0 2S/2W-04R01 340120117051301 7/9/96 1430 300 — 717 7.4 1.6 34.5 19.5 2S/2W-10B02 340106117045001 7/11/96 0930 750 — 510 7.8 7.0 28.5 21.0 2S/2W-11A01 340105117031601 7/15/97 1450 725 — 496 7.8 6.6 — 21.5 2S/2W-11D01 340057117040601 7/15/97 1000 700 — 462 7.8 8.8 — 21.0 2S/2W-14C01 340014117034301 7/17/97 1000 250 — 522 7.6 8.8 — 21.5 2S/2W-14R03 335924117031701 7/17/97 0915 775 — 297 9.3 1.9 — 24.5 Table 3 2S/2W-24L01 335848117024301 7/16/97 0925 2,100 — 346 7.9 5.4 — 23.0 2S/2W-28C021 335829117055201 7/28/97 1620 — — 942 7.6 .0 29.5 24.0

39 See footnote at end of table. .001 .001 .001 .001 .001 .001 .002 .001 .002 .015 .019 .001 .001 .001 .001 .001 .002 .001 .001 .002 .001 .001 .003 .001 .063 (mg/L) Iodide, 0.001 <.001 <.001 <.001 <.001 <.001 dissolved — .04 .05 .07 .17 .04 .04 .04 .04 .04 .04 .04 .13 .05 .13 .09 .12 .09 .07 .14 .07 .06 .04 .04 .09 .08 .08 .13 .07 .07 .38 (mg/L) 0.10 Bromide, dissolved — .7 .5 .8 .8 .6 .6 .6 .6 .6 .6 .6 .5 .5 .6 .4 .7 .5 .5 .5 .6 .6 .5 .5 .9 .6 .9 .5 .5 0.8 6.0 1.0 — (mg/L) Fluoride, dissolved 9.7 6.4 7.3 7.9 8.0 7.0 6.3 7.3 7.9 7.8 6.9 34 11 18 30 32 28 18 36 19 17 17 17 12 15 — 18 16 26 14 11 65 (mg/L) Chloride, dissolved 86 69 39 57 31 28 27 29 29 29 27 24 60 32 29 16 31 29 68 30 31 27 29 74 — 39 36 13 15 14 32 260 (mg/L) Sulfate, dissolved ) 3 , — field 190 220 170 220 200 190 200 180 190 140 170 210 190 230 190 170 200 190 220 160 180 160 170 240 160 160 160 200 100 140 380 Alkalinity (mg/L as CaCO .6 .6 1 2 2 1 1 2 2 2 2 2 2 2 2 2 5 1 2 3 2 2 2 2 2 2 3 2 2 1 2 1 (mg/L) dissolved Potassium, 42 14 16 42 45 25 23 25 28 23 21 24 40 24 33 25 28 25 21 21 22 27 17 23 41 44 39 33 58 39 200 120 (mg/L) Sodium, dissolved .9 1.0 8.5 8.7 8.0 3.5 6.8 18 22 16 15 11 12 12 13 13 13 14 12 23 12 19 20 12 13 22 13 12 12 22 14 17 (mg/L) dissolved Magnesium, 5.8 78 67 53 69 57 59 55 61 63 63 61 61 95 53 62 34 34 68 70 98 63 58 50 61 94 55 46 46 51 28 59 (mg/L) Calcium, dissolved 1 1 3. Chemical and isotopic analyses of water from selected wells in the Yucaipa area, southern California—Continued -25R04 -25R04 -25R04 -25R04 -25R04 -25R04(B) -02M01 -19G01 -27L01 -32C01 -24C02 -25A01 -25R04(B) -34N01 -36G01 -08F01 -15F02 -01J01 -02M01 -03E01 -03L01 -04G03 -04G04 -04J02 -04R01 -10B02 -11A01 -11D01 -14C01 -14R03 -24L01 -28C02 State well number Table 1S/1W 1S/1W 1S/1W 1S/2W 1S/2W 1S/2W 1S/2W 1S/2W 2S/1W 2S/1W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W 2S/2W See footnote at end of table.

40 Surface-Water and Ground-Water Quality in the Yucaipa Area, San Bernardino and Riverside Counties, California, 1996–98 Table 3. Chemical and isotopic analyses of water from selected wells in the Yucaipa area, southern California—Continued Phosphorus Silica, Residue at Nitrite, NO + NO , Ammonia, Ammonia + Phosphorus, Arsenic, Barium, Boron, 2 3 ortho, State well number dissolved 180AC dissolved dissolved dissolved organic, dissolved dissolved dissolved dissolved dissolved (mg/L) (mg/L) (mg/L as N) (mg/L as N) (mg/L as N) (mg/L as N (mg/L as P) (Hg/L) (Hg/L) (Hg/L) (mg/L as P) 1S/1W-19G01 23 485 0.09 13 0.14 0.2 <0.01 0.02 <1 45 70 1S/1W-27L01 20 358 <.01 2.0 .03 <.2 <.01 <.01 <1 12 20 1S/1W-32C01 21 298 .02 5.3 .02 <.2 <.01 .01 <1 16 20 1S/2W-24C02 25 412 <.01 5.6 <.02 <.2 <.01 .02 <1 27 70 1S/2W-25A01 25 359 <.01 4.7 <.02 <.2 .01 .02 <1 19 60 1S/2W-25R04(B) 28 295 <.01 2.0 .03 <.1 <.01 .02 3 17 30 -25R04 28 283 <.01 1.9 .03 <.1 <.01 .02 3 16 40 -25R04 28 305 <.01 2.2 .03 <.1 <.01 .02 3 17 40 -25R04 28 317 <.01 1.9 .02 <.1 <.01 .02 2 18 40 -25R04 28 315 <.01 1.4 .03 <.1 <.01 .02 3 18 50 -25R04 28 303 <.01 1.0 .03 <.1 <.01 .02 3 19 40 -25R04(B) 26 290 .01 2.0 .06 <.1 <.01 <.01 3 16 30 1S/2W-34N01 25 512 <.01 24 .02 <.2 .01 .03 <1 58 30 1S/2W-36G01 26 293 <.01 2.1 <.02 <.2 <.01 .01 <1 15 20 2S/1W-08F01 24 369 <.01 4.2 <.02 <.2 .03 .03 <1 28 20 2S/1W-15F02 17 258 <.01 .06 <.02 <.2 <.01 <.01 <1 24 20 2S/2W-01J011 16 712 .05 5.3 .08 <.1 <.01 .02 <1 8 330 2S/2W-02M01 23 363 <.01 7.9 <.02 <.2 <.01 .01 <1 21 20 -02M01 25 354 <.01 7.8 .03 <.1 <.01 .02 <1 21 20 2S/2W-03E01 24 487 <.01 16 .03 <.2 <.01 .02 <1 27 20 2S/2W-03L01 26 314 <.01 6.7 .03 .2 <.01 .02 <1 15 20 2S/2W-04G03 24 287 <.01 1.6 .03 <.2 .03 .02 <1 23 20 2S/2W-04G04 23 260 .01 1.3 .05 <.1 <.01 .02 <1 17 30 2S/2W-04J02 25 281 <.01 2.6 .03 <.2 <.01 .02 <1 18 20 2S/2W-04R01 25 472 .01 9.6 .03 <.2 .02 .03 <1 29 20 2S/2W-10B02 — — <.01 4.9 .02 <.2 <.01 .01 <1 26 — 2S/2W-11A01 24 318 <.01 5.8 <.02 <.2 .02 .02 <1 24 30 2S/2W-11D01 22 294 <.01 3.9 <.02 <.2 .03 .02 <1 19 20 2S/2W-14C01 26 318 <.01 4.2 <.02 <.2 .03 .03 <1 32 20 2S/2W-14R03 15 186 <.01 1.9 <.02 <.2 <.01 .02 5 5 20 2S/2W-24L01 17 213 <.01 2.0 <.02 <.2 <.01 .01 <1 22 20 Table 3 2S/2W-28C021 22 563 .02 <.05 .44 .3 .01 .13 <1 130 50 See footnote at end of table. 41 42 Table 3. Chemical and isotopic analyses of water from selected wells in the Yucaipa area, southern California—Continued Iron, Lithium, Manganese, Strontium, H-2/H-1 O-18/O-16 Tritium, C-13/C-12 C-14 dissolved,

Surface-Water and Ground-WaterQualityintheYucaipa Area,SanBernardinoandRiverside Counties,California,1996–98 State well number dissolved dissolved dissolved dissolved isotope ratio isotope ratio total isotope ratio (percent modern (Hg/L) (Hg/L) (Hg/L) (Hg/L) (per mil) (per mil) (pCi/L) (per mil) carbon) 1S/1W-19G01 140 5 67 490 −56.5 −8.45 7.3 — — 1S/1W-27L01 <3 4 <1 270 −65.5 −9.69 9.6 — — 1S/1W-32C01 31 <4 6 250 −61.9 −9.24 11 — — 1S/2W-24C02 <3 4 <1 350 −56.1 −8.55 2.8 — — 1S/2W-25A01 9 <4 <1 340 −55.6 −8.19 2.8 — — 1S/2W-25R04(B) <10 <4 <4 250 −60.1 −8.99 2.1 −12.9 86.9 -25R04 <10 <4 <4 230 −63.2 −9.23 3.9 — — -25R04 70 <4 <4 260 −58.1 −8.85 <.3 −13.4 86.1 -25R04 <10 <4 <4 270 −58.8 −8.76 .4 −13.8 85.4 -25R04 34 <4 <4 270 −58.8 −8.68 .8 −13.2 87.3 -25R04 <10 <4 <4 260 −58.4 −8.86 1.4 — — -25R04(B) 19 <4 <4 251 −61.0 −9.07 3.4 — — 1S/2W-34N01 12 <4 2 470 — — 2.4 — — 1S/2W-36G01 <3 <4 <1 230 −60.2 −9.02 2.9 — — 2S/1W-08F01 <3 <4 <1 270 −56.6 −8.46 7.7 — — 2S/1W-15F02 39 <4 5 170 −53.8 −8.11 .6 — — 2S/2W-01J011 2,300 <4 23 362 −67.3 −9.97 7.2 — — 2S/2W-02M01 4 <4 <1 290 — — 4.6 — — -02M01 17 <4 <4 296 −57.8 −8.59 — — — 2S/2W-03E01 8 <4 <1 390 −55.2 −8.41 15 — — 2S/2W-03L01 <3 <4 <1 270 −58.4 −8.65 2.8 — — 2S/2W-04G03 4 <4 <1 260 −57.0 −8.50 <.3 — — 2S/2W-04G04 <10 <4 <4 254 −58.4 −8.63 <.3 — — 2S/2W-04J02 <3 <4 <1 250 −58.0 −8.82 <.3 — — 2S/2W-04R01 22 <4 <1 350 −58.4 −8.64 1.8 — — 2S/2W-10B02 <3 <4 <1 270 −57.8 −8.56 1.9 — — 2S/2W-11A01 <3 <4 <1 260 −58.6 −8.52 2.1 — — 2S/2W-11D01 6 <4 <1 260 −58.7 −8.54 1.2 — — 2S/2W-14C01 <3 <4 <1 230 −55.3 −8.11 .8 — — 2S/2W-14R03 <3 <4 <1 50 −57.5 −8.60 .7 — — 2S/2W-24L01 3 <4 <1 330 −59.9 −8.81 .7 — — 2S/2W-28C021 95 4 410 520 −47.3 −6.35 7.8 — — 1Not a production well.